Sedimentary Properties of the Middle−Upper Eocene...

E. TOKER ET AL.

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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, Turkey3 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

Turkish Journal of Earth Sciences (Turkish J. Earth Sci.), Vol. 21, 2012, p. 335–373. Copyright ©TÜBİTAK

doi:10.3906/yer-0909-8 First published online 31 May 2011

MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY

336

Introduction

Th e Palaeocene–Eocene outcrops mark an important event in the history of basins developed before the neotectonic period, which is a known extensional tectonic regime in west Anatolia. During this time interval also occurred the main deformation and HP/LT metamorphism of the Menderes Massif as a result of burial beneath the Lycian Nappes (Şengör & Yılmaz 1981; Satır & Friedrichsen 1986; Bozkurt & Satır 2000; Bozkurt & Oberhänslı 2001; Sözbilir 2002). Th is Palaeocene–Eocene sedimentary succession rests unconformably on diff erent tectonostratigraphic suites, such as the Lycian Nappes (Özkaya 1991; Şenel 1991; Collins & Robertson 1997, 1998, 1999), the Menderes Massif (Poisson 1976; Özkaya 1990, 1991; Özer et al. 2001) and the Beydağları carbonate platform (Özkaya 1991; Collins & Robertson 1998). Th e initial phase of nappe emplacement occurred during the latest Cretaceous (Collins & Robertson 1998), aft er which sedimentary basins developed on top of the imbricated Lycian basement during the Late Palaeocene–Early Eocene (Şenel 1991). Th e basin fi ll comprises basal conglomerates with clasts derived from the Lycian Nappes, bioclastic platform limestones and clastic turbidites and is interpreted as a supra-allochthonous unit (Sözbilir et al. 2001; Sözbilir 2002), thought to represent a temporal restoration of a passive margin during relative tectonic quiescence (Collins & Robertson 1998).

In this study the Middle–Upper Eocene sequences stratigraphically overlying the Lycian Nappes are represented by the Başçeşme and Varsakayayla formations, and the Kayıköy Formation on the Beydağları carbonate platform (Figures 1 & 2).

Th e purpose of this paper is to provide a facies description and interpretation of the Middle–Upper Eocene Başçeşme, Varsakyayla and Kayıköy formations, to identify the factors that controlled their deposition and to describe the palynological

and foraminifera assemblages of these units that have been widely used in palaeoenvironmental interpretations.

Geological Setting

Th e Middle–Upper Eocene outcrops are distributed in the Çardak-Dazkırı (north of Acıgöl), Burdur (north of Lake Burdur) and Isparta (İncesu and Gönen towns) areas (Figures 1, 3, 4 & 6). Th ese basins are located in the Western Anatolia extensional province characterized by numerous NW–SE-, NE–SW-, E–W-trending basins (Koçyiğit 1984, 2005) and rest on the Mesozoic Lycian Nappes and ophiolites (Sözbilir 2005).

Th e Palaeocene–Eocene sedimentary assemblages of southwestern Anatolia are made up mainly of conglomerate, sandstone, turbiditic sandstone-mudstone alternations, carbonaceous mudstone, bioclastic limestone interbeds and, locally, limestone blocks. Th e sedimentary features of these sedimentary constituents mainly indicate a supra-allochthonous basin type, which developed above the Lycian Nappe package (Sözbilir 2002). Th e supra-allochthonous sediments are separated from the basement rocks by a regional unconformity (Sözbilir 2002).

Following Poisson et al. (2003) the tectonic evolution of the study area and its surroundings can be divided into four main stages. Th ese are in ascending order; (1) closure of the Pamphylian basin and emplacement of Antalya Nappes (Late Cretaceous–Early Palaeocene); (2) emplacement of Lycian Nappes (end of Eocene–Early Oligocene); (3) formation of the Oligocene molasse basins and (4) opening of the Baklan and Acıgöl grabens under NW–SE and N–S extensional regimes.

Deposition in the supra-allochthonous Eocene–Oligocene marine basins in SW Anatolia, was controlled mainly by the emplacement of the Lycian

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

E. TOKER ET AL.

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Nappes in the region at the time. However, the mainly ophiolitic detrital constituents of the Başçeşme, Varsakyayla and Kayıköy formations indicate a Late Eocene synsedimentary emplacement of the ophiolite assemblages of the Lycian Nappes. Th e emplacement of the Lycian Nappes in SW Anatolia continued until the end of the Late Miocene. Field observations in the Burdur and Isparta regions show that ophiolitic allochthonous units of the Lycian Nappes are overthrust on to Early Miocene (Aquitanian–Burdigalian) marine sedimentary units. Multiple overthrust systems of the Lycian Nappes on to the Beydagları autochthonous carbonate and detrital units (Late Palaeocene to Early Miocene) suggest an anticlockwise rotation of the western side of the Isparta Angle. Palaeomagnetic studies (Kissel et al. 1993; van Hinsbergen et al. 2010) indicated that the Lycian block on the western limb of the Isparta Angle rotated anticlockwise by about 40° since the Eocene. Furthermore, the palaeomagnetic data suggest that the dominant tensional forces in the study area mainly trend NW–SE.

Stratigraphy

In this study, our fi eld observations were focused

on three diff erent locations, namely the Middle–

Upper Eocene deposits cropping out in the Çardak-

Dazkırı (Başçeşme Formation), Burdur (Varsakyayla

Formation) and İncesu (Kayıköy Formation) basins.

Th e major geological characteristics of these Eocene

basins are briefl y described below.

Çardak-Dazkırı Basin

Th e Çardak-Dazkırı basin is located north of the

Acıgöl Graben, mainly fi lled by Tertiary sedimentary

sequences and characterized by molasse type clastic

deposits (Figure 1) (Koçyiğit 1984; Göktaş et al. 1989;

Yağmurlu 1994; Akgün & Sözbilir 2001; Sözbilir

2005). Th e Upper Eocene Başçeşme Formation,

exposed near Başçeşme village and fi rst named by

Göktaş et al. (1989), unconformably rests on the

Lycian Nappes (Figure 2) (Göktaş et al. 1989). Th e

formation is composed mainly of a fi ning-upward

Menderes Massif

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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).


338

clastic sedimentary succession, which starts with pebble to cobble conglomerates at the base (Göktaş et al. 1989; Akkiraz 2008; Toker 2009; Toker et al. 2009). Vertically and laterally, these coarse conglomerates display gradual transition to a monotonous alternation of sandstone, mudstone with coal and reef carbonates (Göktaş et al. 1989; Akkiraz et al. 2006; Akkiraz 2008; Toker 2009). Th is internal lithological variation is divided into the following members: the reddish-claret Dazlak conglomerate; the Maden sandstone and coaly mudstone and the Asar limestone with corals, algae and benthic fragments (Figure 3b).

Burdur Basin

Th e Burdur basin is located on the northwestern side of Lake Burdur and fi lled with Tertiary deposits which are divided into supra-allochthonous sediments, the Acıgöl group and neo-autochthonous cover units (Yalçınkaya et al. 1986; Şenel 1997) (Figure 4). Th e pre-Eocene basement comprises ophiolitic melange and olisthostrome of the Lycian Nappes (Poisson 1977). Th e Varsakyayla Formation from around Varsakyayla village, named by Poisson (1977), is well exposed in this area and is mainly made up of locally channellized conglomerates, planar cross-bedded sandstones, massive and locally coaly mudstones and bivalve and gastropod-bearing limestone (Akkiraz 2008). Th e Varsakyayla Formation is linked with the Başçeşme Formation due to the similarities of their sedimentary constituents.

İncesu Basin

Th e İncesu Basin is located in the apex of the Isparta Angle and its deposits crop out around Gönen town to the north of Isparta (Figure 7). Th e Kayıköy Formation, named aft er Kayıköy village, where it is well exposed (Karaman et al. 1989), is generally greyish and includes very poorly sorted conglomerates, amalgamated sandstones with mudstone interbeds (Figures 13 & 14). Th e Kayıköy Formation is turbiditic and is composed mainly of sandstone and shale alternations and also contains clayey and cherty interbeds and conglomerate intercalations dominantly of turbiditic origin. Th e Middle–Late Eocene age of the formation is deduced from its stratigraphic position (Figure 6).

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E. TOKER ET AL.

339

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340

Facies and Facies Associations

In this section, three Eocene formations have been

analyzed in terms of their facies associations. Th ese

associations are based on the facies defi ned on

logged stratigraphic sections and used palynological

data (Figures 8, 9, 11–14). Detailed descriptions of

the sedimentary features and palaeoenvironmental

interpretations of the facies and facies assemblages

are given in Tables 1–4, 7 & 8. Facies classifi cation

of alluvial and fl uvial environments is aft er Miall

(1978), who assigned gravel-bearing successions to

G facies, while sandy and clay facies were assigned

to S and F facies, respectively. Small letters following

the capital letter indicate the textural and structural

characteristic of each facies.

Başçeşme Formation

Th e Başçeşme Formation is well-exposed on the north

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

the other is southwest of Boztümbek Tepe (Figure

3b). Th e Öküztepe section is up to approximately

240 metres thick and extends laterally over a few

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

based on type of individual beds, grain size, primary

sedimentary structures and fossil contents (Table 1).

Field photos also illustrate some of the lithofacies

features of the Başçeşme Formation (Figure 10).

Th is lithofacies diversity was grouped into three

main facies associations: FA1 to FA3 (Table 2). FA1

correlates with the coarse-grained Dazlak Member,

FA2 correlates with the fi ner-grained Maden Member

and FA3 correlates with the carbonate Asar Member

(Figures 8 & 9).

Alluvial Fan Deposits (FA1): Description – Th e

alluvial fan facies association is characterized by

the relative abundance of facies Gmm, Gp, Sg, Sp,

St, Shs (Table 1; Figures 8 & 9). Th e FA1 is generally

made up of conglomerates intercalated with pebbly

sandstones. Th is polygenetic conglomeratic facies

association is commonly reddish and brownish,

pebble to cobble grain size, thick bedded to massive,

poorly-sorted, matrix-supported, with erosive

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E. TOKER ET AL.

341

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rdu

r). L

oca

tio

n o

f m

easu

red

sec

tio

ns,

geo

logi

cal

sect

ion

s an

d s

amp

le l

oca

tio

ns

are

ind

icat

ed.


342

AG

E

SE

RIE

S

FO

RM

AT

ION

TH

ICK

NE

SS

(m)

LITHOLOGY

Mes

ozoi

cP

lioc

ene-

Qua

tern

ary

Kay

ıköy

Pal

aeoc

ene-

Eoc

ene

20-7

085

0

Low

er -

“Mid

dle”

Oli

goce

ne

İnce

su

gravel-sand-clay

limestone

coal


coal

coal

pelagic limestones

coal

neritic and hemipelagiclimestones

Kırladağları series(Beydağları autochthon)

not to scale


100-

200 conglomerate

sandstone-mudstoneblocks of neritic and pelagic

limestones

Kır

lada

ğlar

ıse

ries

conglomerate

AG

E

SE

RIE

S

FO

RM

AT

ION

TH

ICK

NE

SS

(m)

LITHOLOGY

Cre

tace

ous

Kay

ıköy

Pal

aeoc

ene-

Eoc

ene

850

Low

er -

“Mid

dle”

Oli

goce

ne

İnce

su

gravel-sand-clay

coal

neritic limestones

coal

coal

coal

neritic and hemipelagiclimestones,vsandstone,vmarl

Isparta series(Beydağları autochthon)

not to scale

sandstone-mudstone

1000

conglomerate-sandstone-mudstone alternation

Bar

lada

ğse

ries

Pli

ocen

e-Q

uate

rnar

y

trachy-andesite

Low

er-M

iddl

e M

ioce

ne

Bar

lada

ğL

ycia

n na

p.


limestone limestone


230

Del

ikar

ası

Ispa

rta

seri

es

pelagic limestones

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).

E. TOKER ET AL.

343

Kap

ıdağ

Yas

sıvi

ran

Gök

tep

eT

epel

ce

Gün

eyke

nt

Gön

en

İleğ

idağ

01

km

Tın

az t

epe

İğde

cik

Köm

ürlü

k

Del

ikar

kası

hill

İsla

mkö

y

Ata

bey

1989

2447

Gök

tepe

Çap

alı

İnce

su

Keç

ibor

lu

AN

TA

LYA

Med

iter

rane

an

Afy

on0

50 k

mN

Fig

ure

14

Fig

ure

12

Fig

ure

13

Kay

ıköy

For

mat

ion

Mid

dle

Eoc

ene

Del

ikar

kası

For

mat

ion

İnce

suF

orm

atio

n

Lower-“Middle”Oligocene

stud

y ar

ea

Pli

o-Q

uate

rnar

y

faul

t

thru

st f

ault

Lyc

ian

Nap

pes

Bar

lada

ğse

ries

Kır

dağl

arı

seri

es

Ispa

rta

seri

es

Bey DağlarıAutochthon

Ant

alya

Nap

pes

EX

PL

AN

AT

ION

SQ

uate

rnar

yal

luvi

um

volc

anic

s

Mio

cene

sedi

men

ts

mea

sure

dse

ctio

ns

Fig

ure

7.

Sim

pli

fi ed

geo

logi

cal

map

of

no

rth

Gö

nen

To

wn

(m

od

ifi e

d f

rom

Gu

tnic

19

77

; Yağ

mu

rlu

19

94

).


344

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

Facies Description Interpretation

Gmm; massive

conglomerates

granule to cobble size, massive, matrix-supported, chaotic, pebbles are rounded to

sub-rounded, poorly sorted to unsorted, generally erosive basement, irregular top,

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

debris-fl ow deposits

Gp; panar cross-

bedded conglomerates

granule to pebble size clast supported by coarse sandy matrix, subangular and poorly

sorted clasts, sand lenses, generally fi ning upward with erosive base, planar cross

bedded, channel fi ll occurs, reddish-brown coloured; dimensions: bed thickness up to

4 m, lateral extent: few ten metres; intercalated with facies Sr

channel fi ll

Gms, matrix-

supported gravelstone

granule to pebble size clasts supported by sandy matrix, poorly sorted, poorly bedded,

few crudely developed normal to inverse grading,yellowish red coloured,angular

to subangular clasts; dimensions: bed thickness up to 6 m, lateral extent: few tens

metres, intercalated with facies Sb, Sl,Fl and C

debris fl ow to hyper-concentrated

fl ow deposits

Sg, gravelly

sandstones

granule to coarse-grained sandstones, poorly sorted and rounded, cross-laminated,

channel-fi lls, reddish coloured, dimensions; bed thickness up to 20 cm, laterally

extent: few metres, intercalated with facies Gmm, Gp

deposits from sand-dominated

chanellized fl ows

Shs, horizontally

stratifi ed sandstones

medium- to fi ne-grained sandstone, moderately sorted, horizontally stratifi ed

bioturbated, locally ripple laminations on top, locally hematite concretions bearing,

reddish-yellowish red coloured; dimensions: bed thickness up to 30 cm, laterally

extent: few tens of metres, intercalated with facies Gms,Sg

planar bed fl ow, upper fl ow regime

Sr, rippled sandstones

medium- to fi ne-grained sandstone, generally parallel laminated at the bottom and

ripples at the top of bed, lenses with mud, greyish red coloured; dimensions: bed

thickness up to 20 cm, lateral extent: few metres, intercalated with facies Sp, Gmm

subaqeous deposits at lower fl ow

regime

Sp, planar cross-


medium- to fi ne-grained sandstone, moderately sorted, massive bedding, planar

cross-stratifi ed, yellowish red coloured, dimensions: bed thickness up to 25cm,

laterally extent few of metres, intercalated with facies Gmm, Gh

lower fl ow regime, sand waves

Sm, massive

sandstones

medium- to fi ne-grained sandstone, moderately sorted, normal graded, greyish

red coloured; dimensions: bed thickness up to 35 cm; lateral extent: a few metres;

intercalated with facies Gh, Fm

rapid sedimentation, sediment

gravity fl ow

Sf, fosilliferous

sandstones

medium- to coarse-grained sandstone, moderately sorted, planar cross-stratifi ed,

corals, gastropods and bivalves-bearing, greyish red coloured; dimensions: bed

thickness up to 60 cm; lateral extent: a few tens of metres; intercalated with facies Fm

decreasing current velocity

Sc, calcareous

sandstones

medium- to coarse-grained sandstone, massive bedding, calcareous sandstone,

yellow coloured; dimensions: bed thickness up to 5 m; lateral extent: a few metres;

intercalated with facies Sf, Lr

edge of bank platform and shelf

Ls, sandy limestone

Sandy limestone with bioclast, grainstone, fl at bedded, coarse grain size, fossil

fragments such as bivalves, benthic foraminifers, yellowish grey coloured; dimensions:

bed thickness up to 5 m; lateral extent: a few metres; intercalated with facies Lr

sporadic storms and currents

across reef, relatively low wave and

current energy

Fm, massive

mudstone

mudstone, laminated, medium- to coarse-grained sandstone, massive bedding,

greyish yellow coloured; dimensions: bed thickness up to 50 cm; lateral extent: a few

metres; intercalated with facies Sg, Sf

suspension sediments, overbank

deposits, waning currents

Lr, reefal limestones

reefal limestone, fl at bedding, mixing of coarse skeletal fragments such as corals,

bivalves, benthic foraminifers and algal mounds, abundant milliolid association,

greyish yellow coloured; dimensions: bed thickness up to 10 m; lateral extent: a few

tens of metres; intercalated with facies Sc

low energy, sporadic currents and

quiescent shallow water

C, coal-coally

mudstone

coal, horizontally laminated, dark brown-black coloured, abundant plant fragments;

dimensions: bed thickness up to 40 cm; lateral extent: a few tens of metres;

intercalated with facies Sm, Fm

subaerial low energy, channel

overbanks, vegetated swamps

deposits and marsh, coastal plain

E. TOKER ET AL.

345

570

565

575

580

585

590

595

6002

2

2

10

7

1

A20

A18A19

A17

A16A15

A14A13A12A11A10A9A8A7A6A5A4A3A2A1

x

A21A22

L M FMC G P C BSand

m

BA

ŞÇ

EŞ

ME

MA

DE

NA

SA

R

9

11

5

9

380

385

390

395

410

415

420

425

405

430

435

400

4

4

1

3

4

4

1

1111

6

BA

ŞÇ

EŞ

ME

MA

DE

N

L M FMC G P C B

Sand

11

7

2

11

4

4

2

1144

44

11

5

6

6

445

450

455

460

475

480

485

490

470

495

465

440

3

3

3

1

9

1

7

3

3

3

111

1111

9

9

99999

11

MID

DL

E-?

UP

PE

R E

OC

EN

E

505

510

515

520

535

540

545

550

530

555

560

525

9

17

1

5

1

9

1

1

1

3

1

3

11

11

11

11

11

11

3

3

5

5

55

7

9

9

Coord: 25342/94691

MID

.-?U

PP

ER

EO

CE

NE

UP

PE

R E

OC

EN

E

4

6

7

10

190

195

200

205

210

215

220

225

230

235

240

245

L M FMC G P C BSand

BA

ŞÇ

EŞ

ME

DA

ZL

AK

6

6

66

6

6

7

7

7

7

7

MID

DL

E-?

UP

PE

R E

OC

EN

E

315

320

325

330

345

350

355

360

340

365

370

335

7

4

4

5

1

12

4

4

Col

or

LITHOL.

Age

Mem

.F

m.

m

2

11

11

22

5

5

5

5

5555

7

7

7

255

260

265

270

275

280

285

290

295

300

305

310

1

6

137

1

2

4

BA

ŞÇ

EŞ

ME

MA

DE

N

11

1

1

1

11

11

7

6

6

7

7

7

MID

DL

E-?

UP

PE

R E

OC

EN

E

5

10

15

20

25

30

40

35

45

50

55

60

7

1

5

1

4

7

6

1

5

7

BA

ŞÇ

EŞ

ME

DA

ZL

AK

MID

DL

E-?

UP

PE

R E

OC

EN

E

1

5

7

7

7

7

7

7

65

70

75

80

85

90

95

100

105

110

115

120

7

5

74

7

7

7

7

7777777

7

5

6

1

4

130

135

140

145

150

155

160

165

170

175

180

Sand

m

2

5

5

5

6

6

L M FMC G P C BSand

125

250

505

m

5

EXPLANATIONS

coarse conglomerate

medium conglomerate

fine conglomerate

coarse sandstone

sandstone

mudstone

coal

sandy limestone

limestone

coral

benthic foraminifer

bioclast

gastropod

bivalve

channel fill

planar bedding

cross lamination

erosive

gradational

covered

bioturbation

Struct.

pebbly coarse sandstone

pebbly sandstone

fractured

sharp

fining upward

coarsening upward

massive beddingflat bedding

hematite concretions

Loc

.B

ed.

L.B

.S.

1 grey2 greyish yellow

3 greyish green4 greyish red5 yellow6 yellowish red

7 red

9 green

10 cream

11 black

Col

or LITHOLOGY

Age

Mem

.F

m.

Struct.

Loc

.B

ed.

L.B

.S.

Col

or LITHO.

Age

Mem

.F

m.

Struct.

Loc

.B

ed.

L.B

.S.

Col

or LIT.

Age

Mem

.F

m.

Struct.

Loc

.B

ed.

L.B

.S.

Gmm

Gp

Gmm

Gp

Sg

Sg

Shs

Sg

Sg

Gp

Gp

Gp

Sp

Sg

Sg

SgGp

GpSg

Gp

Gp

Gp

Gmm

Sg

Sg

Sp

GpSg

Sp

Gmm

Gmm

Gp

Sg

Gp

Sp

Gp

Gp

Gp

Sp

Gp

Sr

C

Sr

Sm

Gms

C Fm

Sg

Sm

Sm

Fm

C

Sm

Sm

Sp

Fm

Fm

FmSm

Sm

Sm

Sm

Sf

CC

Fm

Sf

Sm

SmFmC

CSf

SmSm

LsSm

Sm

Sm

Fm

FmSm

Gp

Gms

CSm

SmFm

Fm

Sf

SmC

Fm

Fm

SmGp

Gmm

Gp

Sm

Fm

GpSm

Fm

CGms

Sm

Sf

Fm

Fm

GmsC

Sm

Sm

Fm

Gms

CSm

SmGp

SfFm

Sm

Gp

Fm

Sm

SmCCC

C

FmSm

Sm

Sm

C Fm

Sm

Ls

Lr

Lr

Al u

v i a

l F a

n (F

A1

)

Al u

v i a

l F a

n (F

A1

)F

a n

D e

l t a / D

e l t a

F r o

n t (F

A2

)

F a

n D

e l t a

/ D e

l t a F

r o n

t (FA

2)

S h

e l f (F

A3)

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


346

1

L M F M C G P C B

Sand

5

10

15

20

25

30

40

35

45

50

55

60

65

77

7

77777

7

7

7

7

777

7

6

70

75

80

85

90

95

105

100

110

115

120

125

m130

4

4

4

112111

4

4

4

BA

ŞÇ

EŞ

ME

FO

RM

AT

ION

DA

ZL

AK

ME

MB

ER

MA

DE

N M

EM

BE

R

7

7

7

7

7

7

7

7

777

MID

DL

E -

?U

PP

ER

EO

CE

NE

135

140

145

150

155

160

170

165

175

180

185

190

195

L M F M C G P C B

Sand

A/49-50

5

270

275

280

285

290

295

305

300

310

315

320

325

330

MA

DE

N M

EM

.

M.-

? I

PP

ER

EO

C.

2

5

5

5

5

5

5

5

5

5

5

5

5

5

A/51

10

5

A/52

10

10

335

340

345

350

355

360m

BA

ŞÇ

EŞ

ME

FO

RM

AT

ION

AS

AR

ME

ME

R

5

UP

PE

R E

OC

EN

E

4

L M F M C G P C B

Sand

2

4

4

57

4

2

200

205

210

215

220

225

235

230

240

245

250

255

m260

BA

ŞÇ

EŞ

ME

FO

RM

AT

ION

MA

DE

N M

EM

BE

R

MID

DL

E -

?U

PP

ER

EO

CE

NE

5

11

2

2

5

5

5

5

5

4

5

9

9

9

Col

or LITHO.

Fm

.

Age

Mem

. Structures

EXPLANATIONS

coarse conglomerate

medium conglomerate

fine conglomerate

coarse sandstone

sandstone

mudstone

coal

limestone

coral

benthic foraminifer

bioclastgastropod

bivalvechannel fillplanar bedding

covered

imbrication

trough cross-bedding

calcerous sandstone

fractured

erosivegradationalsharp

fining upward


Loc

.B

ed.

Col

or LITHOLOGY

Fm

.

Age

Mem

. Structures

Loc

.B

ed.

Col

or LITHO.

Fm

.

Age

Mem

. Structures

Loc

.B

ed.

L.B.S

.

L.B.S

.

L.B.S

.

1 grey2 greyish yellow4 greyish red5 yellow

6 yellowish red7 red9 green

10 cream11 black

Gmm

Gmm

Sp

Sm

Gmm

Sp

Gp

StGp

Gp

Sp

Gmm

Gmm

Gp

Sp

Gp

Sm

Sm

Fm

Fm

Gp

SpC

Sp

Sm

Sm

Fm

Fm

Gp

Sm

Sm

Shs

Fm

Fm

Sm

Sm

SmC Gmm

Sm

Fm

Sf

Gp

Fm

Sm

Sm

Gp

Sc

Sc

Sc

Sf

Sm

Gp

Sm

Sm

Gp

Sm

Sf

Sm

Sf

Lr

Lr

Al u

vi a

l Fa

n(F

A-1

)D

el t a

Fa

n(F

A-2

)

De

l t a/ D

el t a

Fr o

nt (F

A-2

)

De

ltaF

an

(FA

-2)

Co

as

t al /S

he

l f (FA

-3)

coarsening upward

Figure 9. Measured section of the Başçeşme Formation south of Boztümbek Tepe. See Figure 3b for location.

E. TOKER ET AL.

347

a b

c dc

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.

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


348

bases and irregular tops, generally structureless and

chaotically organized, with sub-rounded to rounded

clasts (Facies Gmm) (Figures 8 & 9). Th ey can be

traced laterally for up to a hundred metres. Th e most

common clast components are black dolomites,

serpentinites, and ophiolitic fragments that are

most probably derived from the Lycian Nappes. Th e

cross-bedded conglomerates are compositionally

the same as the massive conglomerates (Gmm),

but diff er in exhibiting planar cross-bedding (facies

Gp) (Figure 9). Clasts within the conglomerate are

poorly-sorted, within a coarse-grained matrix. Th e

coarse-grained gravelly sandstones (facies Sg) are

commonly observed as interbeds in conglomerates

and are poorly sorted and cross-laminated (Figures

8 & 9). Planar cross-stratifi ed sandstones and trough

cross-bedded sandstones (facies Sp, St) were also

observed in massive conglomerates. Horizontally

stratifi ed bioturbated sandstones (facies Shs) consist

of medium–fi ne-grained sandstones with hematite

concretions and locally ripple laminations on top

(Figure 9).

Interpretation – Th e abundance of matrix-

supported, massive to thick bedded, and scarcity of

internal structures in reddish conglomerates and

sandstone beds of the FA1 indicate mainly debris

fl ow processes of alluvial fan deposition (Reineck &

Singh 1975; Miall 1996). Th e clasts are polygenetic

and derived from basement metamorphic rocks by

dominantly cohesive and stream debris fl ow (Nemec

& Steel 1984; Göktaş et al. 1989; Nemec & Postma

1993; Blair 1999; Sözbilir 2002). All these facies of FA1

suggest deposition in an alluvial fan setting in front of

high ground fed from a Lycian Nappes source area. In

the upper parts of the fan (facies Gmm, Gp, Sg, Sp),

with a steeper gradient, high energy fl ow dominated

and thus, overbank deposits are rarely preserved.

Generally, the FA1 facies association demonstrates a

fi ning upward sequence and laterally passes into fan

deltaic conditions.

Fan-delta/Delta Front Deposits (FA2): Description

– Th e Fan delta/delta front facies association is

composed of Gms, Shs, Sp, Sr, Sf, Sm, Ls, Fm, C

facies (Table 1; Figures 8 & 9). Th e grain size is

highly variable, ranging from fi ne grained to gravel

size. Horizontal lamination, ripples, planar cross-

bedding, normal graded bedding, and bioturbations

are characteristic syn-sedimentary structures and occur at various stratigraphic levels (facies Shs, Sr and Sm) and fragments of fossils such as corals, gastropods and bivalves were also observed in FA2 (facies Sf) (Figure 9). Coarsening-upwards sequences were commonly observed in this facies association. Th e mudstone and coal are intercalated with massive sandstones (facies Sm) (Figure 8). Intercalation of debris fl ow facies such as Gmm and Sp indicates an interfi ngering relationship with FA1.

Interpretation – Th e sand-dominated FA2 facies association was probably deposited in a delta setting at the toe of FA1 where the alluvial fan system is continuous through to a fan delta system. Th is facies association concordantly overlies the alluvial fan sediments (FA1). Coal layers represent quiescent subaerial conditions and the massive, laminated mudstone with shell fragments indicates an alluvial swamp environment.

Shelf Deposits (FA3): Description – Th e shelf facies association is composed of Sf, Sc, Ls, Lr facies varieties (Tables 1 & 2; Figures 8 & 9). Th e sandstones mostly consist of gastropod, bivalve- and bioclast-bearing fossiliferous sandstones and calcareous sandstones (facies Sc and Sf). Sandy limestones with benthic foraminifera and bivalves and reef limestones were observed at the top of FA3. Th e lateral extent of these facies usually exceeds tens of metres.

Interpretation – Th e FA3 facies was probably deposited in a lagoon and shelf environment and is characterized dominantly by sandy limestone and reef limestone. Th is facies association overlies fan delta sediments (FA2). Th e calcareous sandstone (facies Sc) commonly occurs near the seaward edge of the bank platform and shelf. Th e development of this deposit requires sand-size sediments and a means of removing sediment smaller or larger than sand-size material. Th ese requirements coincide with wave action or strong tidal currents in an area of high carbonate production (Tucker & Wright 1990). Th e sandy limestone represents open shelf environments (facies Ls). Th e limestone contains corals, benthic foraminifera and bivalves typical of a shelf environment. However, the presence of abundant milliolid association in packstones indicates back-reef or lagoonal environmental conditions (Toker 2009).

E. TOKER ET AL.

349

Fossil Contents – Benthic foraminifera have been identifi ed, particularly in the FA3 facies association of the Asar Member (Başçeşme Formation) (Figures 8 & 9). Th e Nummulites assemblage, including Nummulites fabianii and Nummulites striatus, was identifi ed and in addition, Fabiania cassis, Eorupertia magna, Halkyardia minima, Spahaerogypsina globulus Asterigerina rotula, Quinqueloculina sp., Asterigerina sp., Discocyclina sp., Cibicides sp., Heterostegina sp., Eponides sp., Amphistegina sp., Alveolina sp., Assilina sp., Halkardia sp., Nummulites sp., Operculina sp., Praebulalveolina sp., Eorupertia sp., Fabiania sp., Neoalveolina sp., Halkyardia sp., Anomalina sp., Mississippina sp., Pararotalia sp., Pyrgo sp., Rotalia sp., Sakesaria sp. and Orbitolites sp., were recorded from reef limestones (Akkiraz et al. 2006; Akkiraz 2008). Th e nummulitids (Nummulites fabianii) indicate Shallow Benthic Zonation (SBZ) 19 or 20 (Less et al. 2008). Heterostegina sp., which is found in the Başçeşme Formation, occurs in SBZ 18-19 and indicates an upper Bartonian–Priabonian age (Özcan et al. 2007). Furthermore, Fabiania cassis, Halkardia sp., Rotalia sp., Miliolids, coralline red algae, corals, gastropods and bivalves in these sections of the Başçeşme Formation indicate a Bartonian–Priabonian age. In this part of the section, a shallow shelf is indicated by the presence of Nummulites and towards deeper water, a distal-middle ramp is indicated by orthophragminid assemblages (Bassi 2005).

Varsakyayla Formation

Th e Varsakyayla Formation is well exposed southwest of the Burdur Basin (Figure 5). One outcrop section has been logged through this formation (Figure 11). Th e section is north of Yukarıcimbilli village and up to approximately 270 m thick (Figure 5a). Sedimentary logs defi ned ten lithofacies based on types of individual beds, grain size, primary sedimentary structures and fossil contents (Table 3). Th e observed lithofacies diversity was classifi ed into three main facies associations: FA4, FA5 and FA6 (Table 4). A further fi ft een samples were analysed palynologically (Table 7).

Fluvial Deposits (FA4): Description – Th e fl uvial facies association (FA4) includes Gh, Sm, Sp, Sr, Fm facies varieties (Table 4; Figure 11). Th e

facies association is predominantly sandy facies

comprising medium- to fi ne-grained, moderately

sorted sandstones, interbedded with conglomerates

and thick-bedded mudstones. Planar cross

bedding, ripple lamination, channel-fi lls, hematite

concretions, plant debris and bioclasts are common

sedimentary structures in the sandstones, together

with sharp, sometimes erosive bases (facies Sp and

Sr). Th e conglomerates have interbeds of sandstones

which are horizontally bedded, poorly sorted and are

supported by a sandy, silty matrix. Clasts are rounded

to well-rounded in the pebble to gravel range (facies

Gh). Th e clasts in the conglomerates are polygenetic

and mainly derived from ophiolites of the Lycian

Nappes. Mudstones in the fl uvial facies are massive

to thick bedded, have sharp contacts at base and top

and contain plant debris (facies Fm). Th e gravel and

medium-sand-dominated units in this facies are

mostly grey.

Interpretation – Th e sandy-muddy dominant facies

association (FA4) contains trough cross-bedding

and fi ning-upward cycles indicating the dominance

of fl uvial distributary system during deposition.

Th e sand and mud dominated facies assemblage is

characterized by a very high proportion of fl oodplain

facies, with fewer channel-fi ll deposits (Nichols

& Fisher 2007). Planar-cross bedding is produced

by the downstream migration of two dimensional

bedforms (Harms et al. 1982). Overbank deposits are

represented by thick-bedded, greyish mudstone.

Fan Delta Deposits (FA5): Description – Th e

fan delta facies association (FA5) is composed of

Gmm, Gh, Sm, Sp, Sf, Sc, Fm lithofacies (Table 3;

Figure 11). Th e coarse-grained gravels in the FA5

facies association consist of matrix-supported,

weakly stratifi ed, massive, poorly sorted, rounded to

subrounded pebble to cobble gravels, (facies Gmm)

with horizontally bedded sandy, silty matrix-support,

erosive bases and locally irregular tops (facies Gh).

Th e FA5 facies association is characterized by mostly

sandy facies (facies Sm, Sp, Sf, Sc) which are medium

to coarse grained, and moderately sorted. Planar

cross-bedding and locally channels are common

sedimentary structures in the sandstones (facies Sp,

Sm). Benthic shell fragments such as shallow water

gastropods and bivalves are abundant in this facies

association, and individual beds are bioturbated and


350

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


Gmm, massive

conglomerates

ganule to cobble size clast, silty, sandy and gravelly matrix-supported, massive and unstratifi ed,

poorly sorted rounded to subrounded, generally erosive basement, locally sand lenses, average

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

debris dlow deposits

Gh, horizontally

bedded conglomerates

ganule to pebble size clasts, supported by sandy, silty matrix, horizontally bedded, rounded to

well rounded, erosive basement and some part irregular top, sand lenses are common, grey-

greyish yellow coloured; dimensions: bed thickness up to 2 m; lateral extent: less than 10 metres;

commonly intercalated with facies Sp, Lr

debris fl ow to

hyper-concentrated

fl ow regime

Sm, massive

sandstones

medium- to coarse-grained sandstone, moderately sorted, massive bedded, locally sand lenses,

fractured, bioclasts, bioturbated, greyish coloured; dimensions: bed thickness up to 1–2 m;

lateral extent: few tens of metres intercalated with facies Sp, Sf

deposits from

lower-concentrated

fl ow regime

Sp, planar cross-


medium- to coarse-grained sandstone, pebbly, poorly sorted, sharp base, planar cross-bedded,

hematite concretions, some part channelized, greyish yellow coloured; dimensions: bed

thickness up to 50 cm; lateral extent: few tens metres; commonly intercalated with facies Gmm,

Sm

mid-channel sand

bars

Sf, fosilliferous

sandstones

medium- to coarse-grained sandstone, moderately sorted, sharp base, cross-stratifed,

gastropods, bivalves bearing, fl at bedded, greyish cream coloured; dimensions: bed thickness

up to1 m; lateral extent: tens of metres; intercalated with Fm

decreasing velociy of

water close to shelf

Sc, calcareous

sandstones

medium- to coarse-grained sandstone, moderately sorted, calcareously, fi ning upward, contains

shell fragments (benthic foraminifera, gastropods, bivalves etc.), sharp base and top, cream

coloured; dimensions: bed thickness up to 1 m; lateral extent: few tens of metres; intercalated

with Lr

sporadic storms,

back-reef zone of

land

Sr, ripple-laminated

sandstones

medium- to fi ne-grained sandstone, moderately to well-sorted, sharp base, fi ning upward, fl at

bedded, parallel laminated at base and rippled laminated on top, grey coloured; dimensions: bed

thickness up to 60 cm; lateral extent: tens of metres; intercalated with Sm, Sp, Fm

subaqeous deposits at

lower fl ow regime

Fm, massive

mudstone

mudstone, massive, sharp at base and top, plant debris, greyish yellow coloured; dimensions:

bed thickness up to 40 cm; lateral extent: tens of metres; intercalated with facies Sp, Sm

lower fl ow regime,

channel

overbank deposits

C, coal-coally

mudstone

coal, carbonaceous mud, dark brown-black coloured, plant remains; dimensions: bed thickness

up to 20 cm; lateral extent: less than 10 metres; intercalated with facies Fm

vegetated swamp

deposits, low energy

fl ow

Lr, reefal limestonelimestone, included gastropods, bivalves, corals and algal mounds, cream coloured; dimensions:

bed thickness up to 3 m; laterally extent: less than 10 meters; intercalated with Sc, Shreef framework, shelf

Table 4. Facies associations of the Varsakyayla Formation.


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

E. TOKER ET AL.

351

L M F M C G P C B

1

1

1

1

11

1

1

1111

1

11111

1

1

1

10

04YC/2804YC/01K04YC/02K

04YC/03K

04YC/04K

04YC/05K

04YC/29

11

0

5

10

15

20

25

30

35

40

45

50

55

Sand

VA

RS

AK

YA

YL

A

MID

DL

E -

? U

PP

ER

EO

CE

NE

2

2

2

5

10

1

1

1

1

1

1

1

1

1

1

1

1

1

11

1

1

1

04YC/3004YC/31

LITHOLOGY

Structures

Loc

.B

ed.

L.B

.S.

75

85

100

105

110

115

120

65

70

80

90

95

m

Fm

.

Age

2

2

5

5

UP

PE

R E

OC

EN

E

1

10

04YC/1404YC/1504YC/1604YC/1704YC/1804YC/1904YC/20

04YC/2104YC/2204YC/23

04YC/37-39

L M F M C G P C B

Sand

265

250

255

260

m

VA

RS

AK

YA

YL

A

1

1

10

UP

PE

R E

OC

EN

E

EXPLANATIONS

coarse conglomerate

medium conglomerate

sandstone

mudstone

limestone

coral

benthic foraminifer

bioclast

gastropod

bivalve

channel fill

calcerous sandstone

fractured

erosive

productive sample

barren sample

gradationalsharp

fining upward


plant debris

ripple lamination


pebbly sandstone

bioturbation

algal mound180

175

170

165

160

155

150

140

130

125

135

145

1

1

1

1

1

1

1

11

1

1

L M F M C G P C B

10

10

Sand

04/YC/36

04/YC/35

04/YC/34

04/YC/33

04/YC/32

245

240

235

230

225

220

215

205

200

190

210

195

m

VA

RS

AK

YA

YL

A

UP

PE

R E

OC

EN

E

1

1

10

04YC/9

04YC/8

04YC/7

4

1

10

10

10

10

10

10

10

04YC/1004YC/1104YC/1204YC/13

04YC/6

04YC/24

04YC/2504YC/26

04YC/27

18560

Col

or

LITHOL.

Structures

Loc

.B

ed.

L.B

.S.

Fm

.

Age

Col

or

LITHOL.

Structures

Loc

.B

ed.

L.B

.S.

Fm

.

Age

Col

or

04/YC/33

04YC/03K

1 grey

2 greyish yellow4 greyish red5 yellow10 cream

F a

n D

e l t a

(FA

-5)

F a

n D

e l t a

(FA

-5)

C o

a s

t a l / S

h e

l f (FA

-6)

Coasta

l/Shelf(F

A-6

)

Sm

SpFm

Sm

Fm

Sm

Fm

Sm

Sr

Sm

Fm

SmFm

Fm

Fm

Fm

Sm

Sf

Sc

Fm

Sm

Sp

SmSr

Gh

Gh

Gh

Gh

Gh

Gmm

Sm

Sc

Sm

Sm

Sr

Sm

Sm

Sm

Sm

Sm

Sp

Sm

Sm

Sp

Sc

Sc

Sm

SpGmm

Gmm

Sc

Lr

Lr

Gmm

Sm

Lr

Lr

Lr

Gmm

Sm

Lr

F l u

v i a

l (FA

-4)

Gmmtrough cross-bedding

Gmm

Figure 11. Measured section of the Varsakyayla Formation north of Yukarıcimbili village. See Figure 3 for location.


352

have sharp bases. Th e fi ner unit (facies Fm) present in FA5 consists of massive to thick bedded mudstone, with grey plant fragments and bioturbation.

Interpretation – Th e FA5 facies association represents deposition in a deepening-upward fan-delta system in the Varsakyayla Formation. FA5 is probably deposited on a fan-delta front and fan-delta slope. Th e fan-delta front facies is characterized by pebble to cobble conglomerates, sandstones in both channelized and nonchannelized horizontally bedded units. Fan-delta slope strata are dominated by extensively bioturbated, locally cross-bedded, coarse sandstones, overlain by sandstone/fossil conglomerate couplets (Figure 11). Th us, the fan-delta slope sandstones record deposition in shoreface to inner-shelf environments (Rigsby 1994).

Shelf Deposits (FA6): Description – Th e shelf facies association (FA6) is composed of Gmm, Sp, Sc, Lr facies (Table 3, Figure 11). Coarser-grained conglomerates are rarely preserved and their lateral extent is very limited in FA6 (facies Gmm). Conglomerates with erosive bases are intercalated with sandstones. Th is facies association dominantly consists of creamy bioclastic limestone (facies Lr). Th e bioclasts include foraminifera, algae, corals and bivalves and consist of beds of dense skeletal limestone rich in miliolid foraminifera and coralline algae alternating with calcareous sandstones (facies Lr, Sc).

Interpretation – Th e FA6 facies association was presumably deposited in a shelf environment. Th e calcareous sandstone with shell fragments was probably deposited in a back-reef sand facies (Figure 11) (Toomey 1981). All the features of the back-reef zone of land fringing platforms are strongly infl uenced by the both water exchange between the open sea and infl ux of river water (Einsele 2000). Limestone composed of corals and algal mounds is called bind stone or frame stone. Th e ratio of organisms comprising the skeleton components of these limestones (facies Lr) exceeds 50%. Th e shelf facies association is characterized by the presence of abundant shallow-marine fauna, as observed in the bioclastic limestone facies of the upper part of the Varsakyayla Formation. Th e marine transgression is also well documented by presence of reef limestones containing rich marine fossils, such as coral reefs, benthic foraminifera and echinoderms.

Palynological Contents – Five palynological

samples were collected from the clastic part of

the Varsakyayla Formation (Figure 5a). However,

only two samples were suitable for palynological

counting. Due to the low diversity and relative

percentages of the species, 175 pollen grains in

one sample and 164 pollen grains in the other one

could be counted (Table 5). In total, 37 spore pollen

species were determined. Only two spore species,

Leiotriletes triangulus and Baculatisporites primarius

ssp. Oligocaenicus, were counted. Th e angiosperm

pollen average is always higher than that of spores

and gymnosperm. Th e pollen species Plicatopollis

plicatus (~13%), Momipites punctatus (~10%)

Momipites quietus (8%), Tricolpopollenites retiformis

(15%) and Tricolpopollenites liblarensis (8%) had

high percentages. Th e other angiosperms had

comparatively lower percentages (1–3%). Marine

Cleistosphaeridium sp. and Cordosphaeridium sp.,

and undiff erentiated dinofl agellate cysts were also

described from the samples (Table 5).

Th e characteristic Early Eocene taxa Normapolles,

such as Basopollis, Interpollis and Urkutipollenites, do

not occur in the Varsakyayla Formation. According

to Riegel et al. (1999), the variety of Normapolles is

higher in the Early Eocene than in the Middle Eocene.

Normapolles were not recorded from the Middle–

?Late Eocene coal occurrences of central Anatolia

by Akyol (1980), Akgün (2002) and Akgün et al.

(2002). However, the species Plicatopollis lunatus,

Triatriopollenites excelsus, Subtriporopollenites

anulatus ssp. nanus and Compositoipollenites

rhizophorus ssp. Burghasungensis, generally observed

in Eocene sediments, were also identifi ed from the

Varsakyayla Formation.

Furthermore, the palynomorph content of the two

samples is similar to the palynomorph content of the

Maden member (Başçeşme Formation) previously

made by Akkiraz et al. (2006). In particular, the

mangrove species Psilatricolporites crassus (Pelliciera)

is present in high percentages in the Maden member

(upper part of the Başçeşme Formation) and also

occurs in the Varsakyayla Formation, as a few grains.

Th e clastic parts of the Varsakyayla Formation are

well correlated with the Maden member (Başçeşme

Formation). However, the diversity of species

obtained from the Varsakyayla Formation is less than

E. TOKER ET AL.

353

Tab

le 5

. Q

uan

tita

tive

co

un

tin

g re

sult

s o

f p

alyn

om

orp

hs

in t

he

Var

sak

yayl

a F

orm

atio

n o

f th

e B

urd

ur

Are

a.

TA

XA

Pal

aeo

veg

etat

ion

Typ

esS

amp

le n

um

ber

s

SP

OR

E

04

/YC

01

04

/YC

02

Lei

otri

lete

s tr

ian

gulu

s

Swam

p -

Fre

shw

ater

1

Ba

cula

tisp

orit

es p

rim

ariu

s ss

p. o

ligo

caei

nu

s(O

smu

nd

acea

e: O

smu

nd

a)

2

GY

MN

OS

PE

RM

OU

S

Pit

yosp

orit

es m

icro

alat

us

(Pin

acea

e: P

inu

s h

aplo

xylo

n t

ype)

Mo

nta

ne

11

4

AN

GIO

SP

ER

MO

US

MO

NO

CO

TY

LE

DO

NE

AE

Are

cipi

tes

bran

den

burg

ensi

s(?

Are

coid

eae,

?P

alm

ae )

Bac

k -

Man

gro

ve1

DIC

OT

YL

ED

ON

EA

E

Tri

atri

opol

len

ites

ru

ren

sis

(M

yric

acea

e: M

yric

a)

Lo

wla

nd

- R

ipar

ian

3

Tri

atri

opol

len

ites

bit

uit

us

(Myr

icac

eae:

Myr

ica

)1

Tri

atri

opol

len

ites

exc

elsu

s ss

p.t

ypic

us

(Myr

icac

eae)

1

Pli

cato

pol

lis

lun

atu

s(J

ugl

and

acea

e)

2

Pli

cato

pol

lis

plic

atu

s(J

ugl

and

acea

e)1

82

5

Mom

ipit

es p

un

ctat

us

(J

ugl

and

acea

e: E

nge

lhar

dia

)

Lo

wla

nd

- R

ipar

ian

14

18

Mom

ipit

es q

uie

tus

(J

ugl

and

acea

e: E

nge

lhar

dia

)1

21

5

Subt

rip

orop

olle

nit

es a

nu

latu

s ss

p. n

anu

s(J

ugl

and

acea

e: ?

Car

ya)

2

Intr

atri

por

opol

len

ites

in

du

bita

libi

s(T

ilia

ceae

)1

Com

pos

itoi

pol

len

ites

rh

izop

hor

us

ssp

. bu

rgh

asu

nge

nsi

s(I

caci

nac

eae)

11

Pol

ypor

opol

len

ites

un

du

losu

s

(U

lmac

eae:

Ulm

us)

1

Tri

colp

opol

len

ites

ret

ifor

mis

(S

alia

ceae

: Sal

ix/P

lata

nu

s)2

92

4

Tri

colp

opol

len

ites

mic

roh

enri

ci

(Fag

acea

e: Q

uer

cus)

43

Tri

colp

opol

len

ites

par

mu

lari

us

(?F

agac

eae,

?E

uco

mm

iace

ae: ?

Eu

com

min

ia)

1

Tri

colp

opol

len

ites

hen

rici

(Fag

acea

e: Q

uer

cus )

Mo

nta

ne

1

Tri

colp

opol

len

ites

libl

aren

sis

ssp

. lib

lare

nsi

s

(?

Fag

acea

e)9

21

Tri

colp

opol

len

ites

libl

aren

sis

ssp

. fal

lax

(?F

agac

eae)

17

7

Tri

colp

orop

olle

nit

es a

sper

(Fag

acea

e: Q

uer

cus)

2

Tri

colp

orop

olle

nit

es p

seu

doc

ingu

lum

(An

acar

dia

ceae

: Rh

us)

1

Tri

colp

orop

olle

nit

es c

ingu

lum

ssp

. ov

ifor

mis

(Fag

acea

e: C

ast

anea

,Ca

stan

opsi

s,L

ith

ocar

pus,

Pa

san

ia)

11

5

Tri

colp

orop

olle

nit

es c

ingu

lum

ssp

. fu

sus

(Tri

gon

aba

lan

us)

Lo

wla

nd

- R

ipar

ian

72

Tri

colp

orop

olle

nit

es c

ingu

lum

ssp

. pu

sill

us

(F

agac

eae:

Ca

stan

ea,C

ast

anop

sis,

Lit

hoc

arpu

s,P

asa

nia

)3

2

Tri

colp

orop

olle

nit

es m

arco

du

ren

sis

(Vit

acea

e: C

issu

s)U

nk

no

wn

1

Tri

colp

orop

olle

nit

es m

ega

exa

ctu

s ss

p.

exa

ctu

s

(C

yril

lace

ae)

23

Tri

colp

orop

olle

nit

es m

ega

exa

ctu

s ss

p. b

rüh

len

sis

(Cyr

illa

ceae

)1

07

Tri

colp

orop

olle

nit

es e

dm

un

di

(M

asti

xiac

eae)

Lo

wla

nd

- R

ipar

ian

1

Tri

colp

orop

olle

nit

es m

icro

reti

cula

tus

(O

leac

eae:

Ole

a, F

raxi

nu

s, L

igu

stru

m)

65

Tri

colp

orop

olle

nit

es o

leoi

des

(O

leac

eae)

1

Tri

colp

orop

olle

nit

es v

ille

nsi

s(C

up

uli

fera

e)

2

Tri

colp

orop

olle

nit

es s

olé

de

por

tai

(?F

abac

eae,

?R

osa

ceae

, ?A

nac

ard

iace

ae)

Un

kn

ow

n

1

Tri

colp

orop

olle

nit

es k

rusc

hi

ssp

. pse

ud

ola

esu

s(N

yssa

ceae

)

1

Psi

latr

icol

por

ites

cra

ssu

s(P

elli

cier

a)

Man

gro

ve2

2

Tet

raco

lpor

opol

len

ites

obs

curu

s(S

apo

tace

ae)

Lo

wla

nd

- R

ipar

ian

1

INC

ER

TA

E C

ED

IS

Cle

isto

sph

aer

idiu

m s

p.

Shal

low

- m

arin

e

1

Cor

dos

pha

erid

ium

sp

.

2

Un

diff

ere

nti

ated

din

ofl

agel

late

cys

ts

34

To

tal

17

51

63


354

in the Maden member (see Akkiraz et al. 2006 for the whole assemblage).

Foraminifera Contents – In this study, thirty-seven

samples suitable for analysis of benthic foraminifera

in the Varsakyayla Formation contained: Nummulites

fabianii Prever, Peneroplis sp., Peneropliidae,

Halkyardia minima, Mississippina sp., Textularia

sp., Planorbulina sp., Linderina? sp., Discorbiidae,

Ditrupa sp., Halkyardia minima Liebus, Eorupertia

magna Le Calvez, and Sphaerogypsina globolus

(Table 6; Figure 11). Haurinidae and Rotaliidae

occur rarely in samples. Also, Nummulites fabianii

(nummulitids) primarily occur in samples 04YC/32–

04YC/36, 04YC/24–04YC/25, 04YC/13–04YC/22

and 04YC/37–04YC/39 (Figure 11). In this study

no orthophraminids have been identifi ed in any of

the sections. Small benthic foraminifera (miliolids),

fragments of bivalves and corals were also observed.

Th e abundance of nummulitids suggests an inner

and middle shelf environment, deposited during late

Middle Bartonian–Priabonian (SBZ 18-20).

Samples between 04YC/06 and 04YC/12 have a

reef character, and do not include Nummulites and

Discocyclina, because these kinds of shallow marine

environments are not their optimal living conditions.

Samples between 04YC/29 and 04YC/31 indicate

a shelf lacustrine environment. Samples 04YC/32–

04YC/36 and 04YC/25–04YC/27 indicate a deeper

marine carbonate shelf environment. Sample 04YC/24

indicates a reef environment. Samples between

04YC/06 and 04YC/11 indicate a shelf environment,

while samples between 04YC/12 and 04YC/23

suggest a deeper shelf environment. Sample 04YC/21

indicates a shallow marine environment. Samples

between 04YC/37 and 04YC/39 suggest a carbonate

shelf environment (Figure 11). Anomaliniidae,

Discorbiidae, Peneropliidae, Textulariidae and

Valvuliniidae were also described from the samples

(Table 6).

Kayıköy Formation

Th e Kayıköy Formation is well-exposed around

Gönen and Atabey towns and İncesu village (Figure 7). Four outcrop sections were logged through the Kayıköy Formation to document its lithological characteristics (Figures 12, 13 & 14a, b). Nine

lithofacies were defi ned, based on type of individual beds, grain size, and sedimentary structures (Table 7). Measured sections were logged in three diff erent places: two from southeast of İncesu, while a third was logged east of Karakaya Tepe and the last section was logged from the northeastern part of Kızıldere north of Gönen (Figures 12–14). Th e lithofacies diversity was grouped into main four main facies associations, FA7 to FA10 (Table 7).

Major Channel Deposits (FA7): Description – Th e major channel facies association (FA7) is characterized by the relative abundance of facies F1, F2, F3, F4, F5 and F6 (Table 8; Figure 12). It is dominated by pebble to cobble grain size conglomerates intercalated with pebbly sandstones. Conglomerates are generally thick-bedded to massive, very poorly sorted, sandy silt matrix-supported, well-rounded, erosively based and amalgamated (Figure 12). Pebbly sandstones are poorly sorted and pebbles and granules are dispersed in a matrix of sand (facies F4). Scours and load casts at the bottom of the bed are common sedimentary structures (Table 7). However, disorganized and stratifi ed sandstones were also observed in the FA7 facies associations (Figure 12).

Interpretation – Th e FA7 facies assemblages, composed of conglomerate and sandstone, represent long distance transport by high concentration turbidity currents or debris fl ows and fi nal rapid sedimentation of all grains (Stanley & Kelling 1978; Nemec et al. 1980). Gravels may slide into place on liquefi ed mud. Some muddy gravel occurrences could have formed from thorough mixing of gravel and mud aft er sliding down a steep slope (Crowell 1957). Stratifi ed sandstones are represented by deposits from traction bed loads or traction carpets at the base of a high-concentration turbidity current (Hendry 1973, 1978; Mutti & Ricci-Lucci 1975; Hein 1982; Hein & Walker 1982; Lowe 1982; Surlyk 1984). Disorganized sandstones were deposited by rapid sedimentation from a high-concentration turbidity current by consolidating a dense cohesionless suspension and/or post-depositional liquefaction to destroy any previously formed sedimentary structures. Grain fl ow processes on steep slopes could form disorganized sands (Piper 1978; Lowe 1982).

Proximal (Upper) Fan Deposits (FA8): Description – Th e proximal (upper) fan facies association (FA8)

E. TOKER ET AL.

355

Bur

dur

Are

a

Sam

ple

For

amin

ifer

a

04YC/01

04YC/02

04YC/0304YC/04

04YC/05

Age

For

mat

ion

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abon

ian

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saky

ayla

Nu

mm

uli

tes

fab

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iiH

alk

yard

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04YC/26

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Not to scale

not to scale

Pli

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Tab

le 6

. O

ccu

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ce o

f p

alyn

om

orp

hs

and

ben

thic

fo

ram

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era

in t

he

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atio

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mp

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oca

tio

n.


356

is characterized by lithofacies F1, F2, F3, F5, F6 and F9 (Table 8 and Figure 13). It consists of massive, pebble to cobble grain size conglomerates, bedded,

disorganized conglomerates and medium- to coarse-grained sandstones. Conglomerates are badly sorted but fi ne upwards, with well-rounded clasts, sharp

1

t

1

1

1

1

1

1

1

1

1

1

1

1

1

11

1

1

1

1

1111

1

1

1111

1144411

11

L M F M C G P C B

Sand

Color Lithology

Structures

LocalbeddingL.B.S.

Fm.Age

5

10

15

20

25

30

40

35

45

50

55

60m

1

1

11

1

4

1

1

1

1

1

1

11

1

1

1

1

1

1

1

11

1

1

1

1

1

1

441111

1

1

1

1

65

70

75

80

85

90

95

100

105

110

115

120m

1

L M F M C G P C B

Sand

Color LithologyStructures

LocalbeddingL.B.S.

Fm.Age

111

11111

1

7

1

KA

YIK

ÖY

MID

DL

E E

OC

EN

E

KA

YIK

ÖY

MID

DL

E E

OC

EN

EM

a j o

r c h

a n

n e

l f a c

i e s

(FA

-7)

M a

j o r c

h a

n n

e l f a

c i e

s (F

A-7

)

F1

F1

F1

F1

F1

F4

F6

F1

F6

F6

F1

F1

F1

F6

F6

F1

F6

F1

F6

F1

F2

F2

F3

F1

F1

F1

F1

F1

F1

F1

F1

F6

F1

F1

F4

F5

F6

F6

03/06G

03/11G

03/10G

Figure 12. Measured section of the Kayıköy Formation in the northeastern part of Kızıl Dere, north of Gönen Town.

E. TOKER ET AL.

357

4

4

1

111

3

4

1

4

SandL M F M C G P C B

5

10

15

20

25

30

40

35

45

50

55

60

KA

YIK

ÖY

MID

DL

E E

OC

EN

E

8

8

88888

8

888888

8

888

8

8

8

8

8

9

65

70

75

80

85

90

95

100

105

110

115

120

125m

Fm

.

Age

4

4

3

5111

114444

4

4

4

444

4

4

144

Col

or

Structures

Loc

alB

ed.

LITHOLOGY

8

888

8

8

8

8

88

8

8

8

130

135

140

165

170

175

180

185

145

150

155

160

190

KA

YIK

ÖY

MID

DL

E E

OC

EN

E

4

4

4

4

4

4

4

1

44

444

4

4

1

4

4

44

4

SandL M F M C G P C B

555

5

5

6

66

6

6

6

888

888

8

4

1

1

411

195

200

205

230

235

240

245

250

210

215

220

225

255m

5

5

66

6

6

6

6

6

666

666

66

666

66

6

8

8

8

8

260

265

270

295

300

305

310

315

275

280

285

290

KA

YIK

ÖY

MID

DL

E E

OC

EN

E

11

1

1

1

1

1

1

1

1

11

15

5

5

5

5

5

5

5

55

5

L M F M C G P C BSand

320

325

330

335

340

345

350

1

1

11

1

4

44

4

4

4

4

44

4

55

EXPLANATIONS

coarse conglomerate

medium sandstone

benthic foraminifera

bioclastchannel fill

fractured

erosivegradationalsharp

fining upward


fine conglomerate

coarse sandstone

coarsening upward

covered


mudstone

L.B

.S.

Fm

.

Age

Col

or

Structures

Loc

alB

ed.

LITHOLOGY

L.B

.S.

m

Fm

.

Age

Col

or

Structures

Loc

alB

ed.

LITHOLOGY

L.B

.S.

1 grey3 greyish green4 greyish red5 yellow

6 yellowish red

8 brown

9 green

F2

F1

F6

F6

F1

F5

F6

F1

F6

F6

F6

F6

F6

F6F1

F6

F1

F5

F6

F1

F3

F9

F5F1

F3F6F6F5

F2

F6

F6

F3

F3

F6

F6

F2

F2F6

F5

F2

F2

F1

F5F2

F6

F6

F6

F2

F1

F6

F5

F5

F2

F2

F2F5

F1F5

F1F6

F6F6

F1

F1

F5

load cast

F6

F3

F6F6

F5

F2

F1

F1

F5

F5

F6F2

F6F6

F6

F5F5

F2

F5

F5

F5

F5

F6

F6F6

F2

F2

F6

F6

F6

F5

F6

F2

F2

F5

F2

F2

F5

F2

F6

F2

F6

F6

F5

F5

F5

F5F6

F2

F3

F5F6

F6

F6F2

F2F1

F5

F5

F1

F6

F5

F2F2F5

amalgamation

Pr o

x i m

a l ( U

pp

er ) F

a n

(FA

8)

Media

l fan lo

be fa

cie

s (F

A9)

Media

l fan d

epositio

nal lo

be fa

cie

s (F

A9)

Media

l fan c

hannele

d fa

cie

s (F

A9)

Media

l fan lo

be fa

cie

s (F

A9)

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


358

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


F1, disorganized

conglomerates

granule to cobble size clasts, very poorly-sorted, well-rounded clasts, sandy, silty

matrix-supported, locally sandstone lenses, non-stratifi ed bedded, fl at basement

and irregular top surface, hematite concretions, grey coloured; dimensions: bed

thickness up to 6 m; lateral extent: less than fi ve metres; intercalated with Sm

subaqueous debris fl ow, long

distance

transport by high

concentration

F2, poorly sorted gravel

with

gravel clusters

granule to cobble size clasts, very poorly-sorted, well-rounded clasts, clast- to

matrix-supported with a coarse-grained sandy matrix, locally iregular clusters of

cobble to boulder size clasts, erosive base, locally normal graded, green-brown

coloured; dimensions: bed thickness up to 4 m; laterally extent: few tens of metres;

intercalated with facies F5

rapid deposition from

turbulent

hyperconcentrated fl ows and

coarser

gravel clusters; refl ect

hydraulic

lateral grain size segregation

F3, normal graded

gravels

granule to pebble size clasts, normally graded clast-supported by medium- to

coarse-grained sand, sandy matrix, moderately to poorly sorted, well-rounded clasts,

locally erosive basement, commonly fi ning upward, greyish coloured; dimensions:

bed thickness up to 1 m; lateral extent: few tens of metres; intercalated with facies

deposition by waning

high-density turbidity fl ows

F4, disorganized pebbly

sandstones

medium- to coarse-grained sandstone, pebbly, massive bedded, poorly sorted, fl at

based and irregular upper surface common structures are scours and load casts at

the bottom of bed, greyish

coloured; dimensions: bed thickness up to 2 m; lateral extent: less than ten metres

long-distance transport by

high concentration turbidity

current;

rapid collective grain

deposition of a pebble-sand

F5, disorganized

sandstones

medium- to coarse-grained sandstone with sharp fl at undulose or loaded base,

gravel lenses in some part bioclasts, bioturbated, amalgamated, greyish, yellowish

red coloured; dimensions: bed thickness up to 70 cm; lateral extent: few metres;

intercalated with facies F2, F6

rapid deposition from high

concentration turbidity

current

F6, stratifi ed sandstones

medium- to coarse-grained sandstone, moderately cemented, matrix-supported,

parallel stratifi ed, locally normal to inverse graded, locally gravel lenses, benthic

foraminifera fragments, greyish coloured, dimensions; bed thickness up to 2 m,

laterally extent few metres, intercalated with facies F5

traction bed load of high


current

F7, thick bedded

sandstone-mudstone

couplets

medium-grained sandstone-mudstone couplets, medium -thick- bedded, well-

developed normal graded, sand/mud ratio is high, generally sharp base, contact,

locally erosive base, partly sandstone lenses visible in mudstone, pervasive Tabc

Bouma divisions are present, load structures in sandstones and parallel laminations,

amalgamations, yellowish coloured, sand; lateral extent: few metres

deposition by high-


current

F8, thin bedded

sandstone-mudstone

couplets

medium-grained sandstone-mudstone couplets, medium-thick-bedded, well-sorted,

well-developed normal graded, sand/mud ratio is low, generally sharp base, contact,

locally erosive base, partly sandstone lenses visible in mudstone, pervasive Tabc

Bouma divisions are present, load structures in sandstones and parallel laminations,

amalgamations, yellowish coloured; lateral

extent: few metres

deposition by low-density

turbidity currents

F9, mudstone/shale

mudstone, fl at bedded partly massive, sharp base and upper surface, parallel

lamination on top, fractured, burrows, grey coloured; dimensions: bed thickness up

to 2 m; lateral extent: tens of metres; intercalated with facies

deposited suspension of low-

density turbidity

currents

bases, contain benthic shell fragments and are

intercalated with sandstones (facies F1) (Figure 13).

Th e sandstones are poorly-sorted, fl at based and

bioturbated. Most of them have scoured surfaces, and

bed amalgamation is present (Figure 13).

Interpretation – Th e massive, disorganized

conglomerates of the Kayıköy Formation are

considered to be debris fl ow deposits in the proximal

(upper) fan (FA8), associated thin alternating sand

and mud deposits that can be interpreted as overbank

E. TOKER ET AL.

359

deposits. Similar disorganized conglomerates can be

interpreted as relating to deposition within either the

proximal (upper) fan or proximal parts of the medial

fan distributary channels (Table 7; Figure 13). All

these coarse clastics represent high-concentration,

turbidity currents (Mutti & Ricci-Lucci 1975).

Medial Fan Deposits (FA9): Description – Th e

medial fan facies association (FA9) includes the F1,

F2, F3, F5 and F6 facies varieties (Table 7, Figure 13).

Medial fan deposits were observed as two diff erent

facies, namely the medial fan channel facies and

medial fan depositional lobe facies. Th e medial fan

channel facies is characterized by massive poorly-

sorted conglomerates, with well-rounded clasts, sharp

bases and locally irregular tops, hematite concretions

and bioclasts (Figure 13). Th e depositional lobe

facies is composed of medium- to coarse-grained,

thick-bedded, parallel stratifi ed, non-channelized,

thickening-upward sandstones with load casts,

(facies F5 and F6; Figure 13). Th ese thick-bedded

sandstones are characterized by classical Bouma

sequences but complete Bouma sequences are absent.

Most of the beds consists of Ta-c

Bouma sequences,

whereas the Tb, T

ab, T

bc/e divisions are less commonly

observed. Th e sand/mud ratio of these deposits is

very high and bed amalgamation is typical.

Interpretation – Th e middle fan association (FA9)

is also a combination of channel-fi ll deposits (facies

F1), interchannel deposits (facies F2, F3, F4) and

overbank deposits (facies F6 and F9). Th e sandstones,

with sharp, scoured to fl at bases, normal grading and

parallel laminated tops, suggest deposition from

traction bed loads or traction carpets at the base

of a high- concentration turbidity current (Hendry

1973, 1978; Hein 1982; Hein & Walker 1982; Lowe

1982; Surlyk 1984). Th e base-missing sandstone beds (T

b, T

bc) are interpreted as the deposits

of low-concentration turbidity currents (Lowe 1982). Th e medial fan depositional lobes occur as thickening-upward and thinning-upward sequences which correspond to lobe progradation and lobe abandonment, respectively.

Distal Fan Deposits (FA10): Description – Th e distal fan association (FA10) includes facies F1, F6, F7, F8 and F9 (Table 8; Figure 14a, b) and is dominated by moderately thick, massive mudstone with thin (0.5–5 cm), fi ne-grained sandstones which are massive, or exhibit Bouma T

d/e sequences

characteristic of this facies. Th e sandstone beds show typical base-missing Bouma sequences, such as T

d/e,

Tb-e

, Tb/e

. Th e sandstone/mud ratio is less than 1. Th e lower contacts of sandstone beds are sharp, whereas the upper contact of the same beds is gradational with overlying mud beds (Figure 14b).

Interpretation – Th e distal fan facies association (FA10) comprises thin and fi ne turbidites (facies F8 and facies F9) and mud interbedded with base-missing sandstone beds. Th ey were probably deposited by low-concentration turbulent fl ows far from channel sources (Bouma 1962, 1964; Stow et al. 1996; Einsele 2000).

Formanifera Contents – Th e Kayıköy Formation is characterized by a lack of fossil content and only yielded a few fossil samples, such as Nummulites sp., Assilina sp., Discocyclina sp., Rotaliidae and Nodosariidae (Plate 3). Some samples also contain planktonic foraminifera, such as Globigerina sp., and Globigerinidae. Th is formation is repesented by fl ysch deposits containing planktonic foraminifera and thin-bedded mudstone-sandstone alternations.

Table 8. Facies associations of the Kayıköy Formation.


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


360

1

11

111111

1

444

11411

11

4141

1

1

1

114

4

1

1

1111

1

L M F M C G P C B

Sand

5

10

15

20

25

30

40

35

45

50

55

60 5

5

5

5555

55

5

1

11

1

1

1

1111111111114

4

1

1

4

11444

1

4

1

1

1

44

4

4

1

1

1111

125

120

115

110

105

100

95

90

85

80

75

70

65

m

55

5

555

555

5

5

1

KA

YIK

ÖY

F

MID

DL

E E

OC

EN

E

1

1130

Col

or LITHOLOGYStructures

Loc

.B

ed.

L.B

.S.

Fm

.

Age

0,5

1

1,5

2,5

3,5

4m

Fm

.

Age

Col

or Structures

L.B.S.Localbedding

1

1

111

1

1

1

6

1

5

1

1

1

1

77

7

7

6

6

1

8

1

1

1

8

1

L M F M C G P C BSand

KA

YIK

ÖY

MID

DL

E E

OC

EN

E

LITHOLOGY

3

2

b

EXPLANATIONSmedium conglomerate

medium sandstone

mudstone

bioclast

fractured

erosive

gradationalsharp

fining (thinning)upward


plant debris


bioturbation

fine conglomerate

coal

covered

laminated

load castfine sandstone

coarse sandstone

1 grey4 greyish red5 yellow

6 yellowish red

7 red

8 brown

F6

F1

F9

F7

F8

F8

F6

F6

F6

F7

F8

F8

Dis

tal F

an /B

asin

pla

in“fly

sch”

(FA

-10)

Me

dia

l fan

(FA

-9)

a

F9

F6F1

F1

F9

F9

F9

F9F6

F8

F9

F9

F9

F6

F5

F6

F6

F6

F7

F7

F8

F8

F8

F9

F9

F9

F9

F9

F9

F9

F9

F9

F6

F6

F6

F9

Dis

tal F

an /B

asin

pla

in“fly

sch”

(FA

-10)

Dis

tal F

an /B

asin

pla

in“fly

sch”

(FA

-10)

trace fossil

burrow

coarsening (thickening)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.

E. TOKER ET AL.

361

Depositional Systems

Th e collected data, comprising a preliminary facies

analysis of the Middle–Late Eocene terrigenous

sequences of the Başçeşme, Varsakyayla and Kayıköy

formations, and tectonic structures which have

progressively aff ected these transgressive deposits, let

us establish a palaeoenvironmental model. Figures

15–17 schematically illustrate the depositional

system in the Başçeşme, Varsakyayla and Kayıköy

formations, based on the data presented so far. Th e

deepening trends of these units and correlation of the

sections, based on facies relations and fossil contents,

can be shown in block diagrams.

Th e Çardak-Dazkırı area was aff ected by post-

orogenic tectonic processes (Koçyiğit 1984; Göktaş et

al. 1989; Sözbilir 2005). Th erefore, providing detailed

facies analysis and palaeontological data is very useful in order to understand the palaeoenvironmental history of this basin. Th e basal part of the Eocene deposits in this basin is composed of transgressive units. Th is transgressive sedimentation started with the Dazlak member (FA1) (Başçeşme Formation) while the prograding fan delta and shelf deposits are represented by the Maden (FA2) and Asar members (FA3) (Başçeşme Formation). Th e Dazlak member, deposited mostly by debris fl ow processes of alluvial fan deposits, consists of a thick unfossiliferous polygenetic conglomeratic succession. Fan deltaic sandstone-mudstones intercalated with coal seams (Maden member) grade up into shallower marine sandstones and reef limestones (Asar member) in the Bartonian–Priabonian. In the upper part of the Asar Member the foraminifera Fabiania cassis, Eorupertia

alluvial fan

fan delta

(reef)

Lycian Nappes

FA1

N

FA2

FA3

shelf

(debris flow)

(delta front)

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.


362

magna, Halkyardia minima, Sphaerogypsina globulus Asterigerina rotula, Quinqueloculina sp., Asterigerina sp., Discocyclina sp., Cibicides sp., Heterostegina sp., Eponides sp., Amphistegina sp., Alveolina sp., Assilina sp., Halkardia sp., Nummulites sp., Operculina sp., Praebulalveolina sp., Eorupertia sp., Fabiania sp., Neoalveolina sp., Halkyardia sp., Anomalina sp., Mississippina sp., Pararotalia sp., Pyrgo sp., Rotalia sp., Sakesaria sp. and Orbitolites sp., indicate an inner to middle shelf environment.

Th e other Eocene outcrop located in the Burdur area is a transgressive deposit starting with the Varsakyayla Formation. Th e basal part of the Varsakyayla Formation is composed mainly of sandstones with trough and planar cross-bedding and ripple lamination and mudstones with plant debris. Th ese unfossiliferous clastic deposits represent a fl uvial environment (FA4) and change up-section to fi ne-grained fan-deltaic (FA5) and shallow marine (FA6) sediments containing small benthic foraminifera, coral reefs and echinoderms in the late

Bartonian–Early Priabonian. A benthic foraminifer

assemblage, Nummulites fabianii Prever, Peneroplis

sp., Peneropliidae, Halkyardia minima, Mississippina

sp., Textularia sp., Planorbulina sp., Linderina? sp.,

Discorbiidae, Ditrupa sp., Halkyardia minima Liebus,

Eorupertia magna Le Calvez, and Sphaerogypsina

globolus from the uppermost part of the sequence

records an inner and middle shelf environment.

In the eastern part of the study area in the

Isparta region, marine conglomerate, sandstone and

mudstone (Kayıköy Formation) was deposited in a

fl ysch-like unstable basin. Major channel facies (FA7)

changes to the lateral and medial fan association

(channel and depositonal lobe facies) (FA9) and distal

fan (thin-bedded sandstone-mudstone alternations)

association (FA10). Fossils from the Kayıköy

Formation indicate a depositional environment

in which the benthic foraminifera, Nummulites

sp., Assilina sp., Discocyclina sp., Rotaliidae and

Nodosariidae are rarely found, although planktons

Lycian Nappes

FA4

N

FA5 FA6

Flood plain

bed loaddeposit

fluvial environment(flood plain, channel fill deposits)

fan delta(fan delta front-fan delta slope)

shelf environment(back reef)

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.

E. TOKER ET AL.

363

alluvial fan

fan delta

(reef)

Lycian Nappes

FA1

N

FA2

FA3

Lycian Nappes

FA4

N

FA5 FA6

flood plain

bed loaddeposit

fluvial environment(flood plain, channel fill deposits)

fan delta(fan delta front-fan delta slope)

shelf environment(back reef)

shelf

(debris flow)

(delta front)

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

Kayıköy Formation during the Eocene.


364

like Globigerina sp., and Globigerinidae are frequently

present in these transgressive deposits.

In the study areas, Bartonian–Priabonian deepening trends may result from global sea level changes, as well as post-orogenic tectonic movements. During the Middle–Late Eocene, the transgressive sedimentation in these basins caused by rising sea level can be linked to global warming eff ects. Th is climatic change is detected by palynofl oral features. Th e mangrove species Psilatricolporites crassus (Pelliciera) occurs in the palynofl ora of the Varsakyayla Formation and this indicates warm climatic conditions, as the mangroves need a tropical and humid climate to develop (Frederiksen 1985; Westgate & Gee 1990). In addition only planktonic foraminiferal fauna was found in the Kayıköy Formation.

Conclusions

Th is paper presents a new aspect of the interpretation of the Middle–Late Eocene sedimentary evolution of the Başçeşme, Varsakyayla and Kayıköy formations. Th ree Eocene formations in SW Turkey: the Başçeşme Formation (north of Acıgöl), the Varsakyayla Formation (north of Lake Burdur) and the Kayıköy Formation (north of Isparta) were all investigated sedimentologically, palynologically and palaeontologically.

• Detailed observations showed that within the Başçeşme, Varsakyayla and Kayıköy formations are thirty-three lithofacies, which can be grouped into ten facies associations. Th e fi rst depositional setting is represented by the alluvial fan, fan-delta and shallow marine settings in the Başçeşme Formation, which can be well correlated with the middle and upper part of the Varsakyayla Formation. Th e Kayıköy Formation is dominantly

characterized by fl ysch-type sandstone-mudstone

alternations.

• Coaly seams of the Başçeşme and Varsakyayla

formations were deposited during the Middle–

?Late Eocene, as indicated by the presence of

stratigraphically important species such as

Aglaoreidia cyclops, Triatriopollenites excelsus,

Subtriporopollenites anulatus ssp. nanus,

Subtriporopollenites constans, Plicatopollis

lunatus, Compositoipollenites rhizophorus

ssp. burghasungensis and Nowemprojectus

tumanganicus.

• Palaeoclimatically, the mixture of temperate

and tropical taxa indicates that from the coastal

to montane environments prevailed during the

Middle–Late Eocene. Th e presence of warm

Tethys waters permitted growth of mangroves in

western Anatolia at this time.

• Benthic foraminiferal fauna such as Nummulites

fabianii (nummulitids), deposited in an inner-

middle shelf environment, indicates a Late

Bartonian–Priabonian age in the Varsakyayla

Formation. However, the orthophragmines (with

genera Discocyclina) indicate a Priabonian age

and deposition on a distal shelf. Th e Kayıköy

Formation is characterized by Globigerina

sp. and Globigerinidae planktic foraminifera,

indicative of a marine environment. Th e variation

of the depositional environment is interpreted as

a result of the sea level changes in the western

Taurides.

Acknowledgements

We thank Dr. André Poisson for his helpful

constructive remarks for the revision of the

manuscript and improvement of the English. Th e

authors thank Ercan Özcan, Ali Aydın, Ömer Elitok

and two anonymous reviewers for their invaluable

criticisms and comments that improved an early

version of the paper.

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Akgün, F. 2002. Stratigraphic and palaeoenvironmental signifi cance

of Eocene palynomorphs of the Çorum-Amasya area in the

central Anatolia, Turkey. Acta Palaeontologica Sinica 41, 576–

591.

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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)

E. TOKER ET AL.

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2

3

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9

8


370

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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7

6

8

9

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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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4

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3

800μm

200μm350μm

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