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E. TOKER ET AL.
335
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.
337
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
Denizli
BodrumMuğla
Tavas
Lycian Nappes
Kos
Göcek
Fethiye
Kaş
AntalyaSerik
Akseki
Seydişehir
Beyşehir
Eğridir
IspartaSultan
Dağ
Burdur
Hadım
Korkuteli
Kemer
Alanya
Alanya M
assif
Bey Dağları
Fenike
Homa
0 25km
N Quaternary
Tertiary basins
Bey Dağları Autochthon
Marine Miocene
Menderes Massif
Antalya Nappes
Alanya Massif
Hadım Nappes
Lycian Nappes
ophiolites
thrust fault
Had
ımN
appes
1
2
3
4
5
N
0 200
Km
Black Sea
Greater Caucasus
NORTHANATOLIAN PROV NI CE
NAFZ
Bitlis-ZagrosSuture Zone
East Anatoliancontractionalprovince
ARABIANPLATE
EAFZANATOLIAN
PLATE
NEA
FZ
DS
FZ
AFRICANPLATE
Mediterranian Sea
Africa
AegeanA
rc
EURASIANPLATE
.
Pliny Strabo
Cyprus
Cyprean Arc
West Anatolianextensionalprovince
MediterranianRidge
Aegean Sea
Isparta.BG
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).
MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY
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).
AG
E
GR
OU
P
FO
RM
AT
ION
TH
ICK
NE
SS
(m)
LITHOLOGY
Mes
ozoi
cQ
uate
rnar
yL
ate
Mid
.Pli
o.
Çam
eli
allu
vium
Boz
dağ
Tok
çaH
ayre
ttin
Çar
dak
Arm
utal
anı
Baş
çeşm
e
?Lut
etia
n-P
riab
onia
n
800
300
200
1500
2000
500
650
Oli
goce
ne
Acı
göl
gravel-sand-clay
clayey limestonetravertine
mudstone-sandstoneconglomerate
sandstone-mudstonelimestone
sandstone-mudstone
sandstone-mudstoneconglomerate
reefal limestone
coal
conglomeratesandstone-mudstone
reefal limestone
coal
conglomerate-sandstone
sandstone-mudstoneconglomerate
reefal limestone
sandstone-mudstonecoal
limestone
sandstone-mudstonecoal
conglomerate-sandstone
Lycian clastics and carbonates
not to scale
Figure 2. Generalized lithostratigraphic columnar section of
the Çardak-Dazkırı basin (modifi ed from Şenel 1997;
Sözbilir 2005).
E. TOKER ET AL.
339
333720
62
30
65
5265
050
0m
55
4854
56 5848
18
54
55
59
47 56
N
EX
PL
AN
AT
ION
Low
er O
ligo
cene
Mio
cene
Qua
tern
aryal
luvi
um
Kız
ılör
en F
orm
atio
n
Arm
utal
anı
For
mat
ion
Asa
r m
embe
r
Mad
en m
embe
r
Daz
lak
mem
ber
Middle-Upper Eocene
BaşçeşmeFormation
norm
al f
ault
stri
ke-s
lip
faul
t
58di
p an
d st
rike
of
bed
sync
line
axi
s
loca
tion
of
the
mea
sure
dse
ctio
ns (
open
cir
cles
sho
ws
begi
nnin
g of
the
sec
tion
)
Fig
ure
8
40
1824
28
22
35
26
40
cont
act
Ökü
z te
pe
Daz
lak
tepe
Boz
tüm
bek
tepe
1181
1014
Fig
ure
9
b
sam
ple
loca
tion
s
N
Kay
aköy
dol
omit
e
Kar
aova
For
mat
ion
LycianNappes
Triassic
Bakla
n
Bo
ğa
ziç
i
Hayre
ttin A
vdan
Arm
uta
lan
ı
Bozkurt
Çard
ak
a0
100 m
Fig
ure
3.
(a)
Geo
logi
cal
map
of
the
Çar
dak
-Daz
kır
ı ar
ea.
(b)
Det
aile
d g
eolo
gica
l m
ap o
f th
e st
ud
ied
are
a, n
ort
h o
f B
aşçe
şme
vill
age.
Lo
cati
on
s o
f m
easu
red
sec
tio
ns
are
ind
icat
ed.
MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY
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
AG
E
GR
OU
P
FO
RM
AT
ION
TH
ICK
NE
SS
(m)
LITHOLOGY
Mes
ozoi
cQ
uate
rnar
yA
quit
ania
n
Aks
ual
luvi
umK
avak
Ard
ıçlı
Sar
aycı
kV
arsa
kyay
la
?Lut
etia
n-P
riab
onia
n
270
150
1000
-150
015
015
00
Oli
goce
ne
Acı
göl
gravel-sand-clay
mudstone-sandstoneconglomerate
coal
recrystalized limestone
sandstone-mudstone
reefal limestone
sandstone-mudstone-limestone
limestone
coal
Lycian clastics and carbonates
reefal limestone
conglomerate-sandstone-mudstonereefal limestone
coalreefal limestone
conglomeratesandstone-mudstone
recristalized limestone
conglomeratesandstone-mudstone
sandstone-mudstone
not to scale
Figure 4. Generalized lithostratigraphic columnar section of the
Burdur basin (modifi ed from Yalçınkaya et al. 1986;
Şenel 1997).
E. TOKER ET AL.
341
Yel
alan
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Ova
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irm
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ere
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ir
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ian
Nap
pes
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For
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ion
allu
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Mio
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For
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AN
AT
ION
S
Gök
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Acıgöl GroupN
AN
TA
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Med
iter
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an
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on0
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m
Dik
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pe
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İnek
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ill
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For
mat
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Lyc
ian
Nap
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Fig
ure
11
loca
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of
the
mea
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d se
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how
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For
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Fig
ure
5b
a
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Fig
ure
5.
(a)
Geo
logi
cal
map
of
the
no
rth
ern
par
t o
f L
ake
Bu
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r (m
od
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rom
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led
geo
logi
cal
map
of
the
no
rth
ern
sid
e o
f
Yu
kar
ıcim
bil
i vi
llag
e (n
ort
h o
f L
ake
Bu
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oca
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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.
MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY
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
conglomeratesandstone-mudstone
coal
coal
pelagic limestones
coal
neritic and hemipelagiclimestones
Kırladağları series(Beydağları autochthon)
not to scale
conglomeratesandstone-mudstone
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
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trachy-andesite
Low
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Bar
lada
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n na
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conglomeratesandstone-mudstone
limestone limestone
conglomeratesandstone-mudstone
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
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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
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Kır
dağl
arı
seri
es
Ispa
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seri
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Bey DağlarıAutochthon
Ant
alya
Nap
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EX
PL
AN
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SQ
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rnar
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luvi
um
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anic
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Mio
cene
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mea
sure
dse
ctio
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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
).
MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY
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-
stratifi ed sandstones
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.
MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY
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
massive beddingflat bedding
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
MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY
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
MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY
350
Table 3. Description and environmental interpretation for the lithofacies in the Varsakyayla Formation.
Facies Description Interpretation
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-
stratifi ed sandstones
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.
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
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
massive beddingflat bedding
plant debris
ripple lamination
hematite concretions
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.
MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY
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
MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY
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
Pri
abon
ian
Var
saky
ayla
Nu
mm
uli
tes
fab
ian
iiH
alk
yard
ia m
inim
a
Eo
rup
erti
a m
ag
na
Nu
mm
uli
tes
sp.
Pa
raro
tali
a.
sp
Op
ercu
lin
a.
sp
Qu
inq
uel
ocu
lin
asp
.
Tex
tula
ria
sp.
Ast
erig
erin
a.
spE
oru
per
tia
sp.
Rot
alii
dae
Tex
tula
riid
ae
Hau
erin
iida
e
Bur
dur
Are
a
Sam
ple For
amin
ifer
a
Bar
toni
anA
ge
For
mat
ion
Pri
abon
ian
Var
saky
ayla
Nu
mm
uli
tes
fab
ian
ii
Ast
erig
erin
a.
sp
Ha
lkya
rdia
min
ima
Eu
per
tia
ma
gn
a
Sp
ha
ero
gyp
sin
a g
lob
ulu
s
04YC/2904YC/3004YC/3104YC/3204YC/3304YC/3404YC/3504YC/3604YC/2404YC/25
04YC/26
04YC/2704YC/0604YC/0704YC/0804YC/0904YC/1004YC/1104YC/12
04YC/1304YC/1404YC/1504YC/1604YC/1704YC/1804YC/1904YC/2004YC/2204YC/2304YC/3704YC/3804YC/39
An
om
ali
na
sp.
Am
ph
iste
gin
asp
.
Nu
mm
uli
tes
sp.
Pa
raro
tali
a.
sp
Mis
siss
ipp
ina
.sp
Rot
alii
dae
Tex
tula
riid
ae
Op
ercu
lin
a.
sp
Het
erost
egin
asp
.
Qu
inq
uel
ocu
lin
asp
.
Hau
erin
iida
e
Pyr
go
.sp
Pen
erop
liid
ae
Tex
tula
ria
sp.
Dis
corb
iida
e
Val
vuli
niid
ae
Pen
eropli
ssp
.
Pla
norb
uli
na
sp.
Lin
der
ina?
sp.
Gyp
sina
sp.
Ano
mal
inii
dae
Ep
on
ides
sp.
Eth
elia
sp.
Pal
ynom
orhp
sL
eiotr
ilet
es t
riangulu
s
Bacu
lati
spori
s pri
mari
us
ssp. oli
gaca
enic
us
Pit
yosp
ori
tes
mic
roala
tus
Are
cipit
es b
urg
hasu
ngen
sis
Tri
colp
oro
po
llen
ites
meg
aex
act
us
exa
ctu
sss
p.
04YC/01K04YC/02K
Tri
atr
iopoll
enit
es r
ure
nsi
s
Tri
atr
ipoll
enit
es b
ituit
us
Tri
atr
ipoll
ebit
es e
xcel
sus
typic
us
ssp.
Pli
cato
poll
is l
unatu
s
Mom
ipit
es p
unct
atu
s
Mom
ipit
es q
uie
tus
Subtr
iporo
poll
enit
es a
nula
tus
nanus
ssp.
Com
posi
toip
oll
enit
es r
hiz
ophoru
sburg
hasu
ngen
sis
ssp.
Intr
atr
iporo
poll
enit
es i
ndubit
ali
bis
Poly
poro
poll
enit
es u
ndulo
sus
Tri
colp
opoll
enit
es r
etif
orm
is
Tri
colp
opoll
enit
es m
icro
hen
rici
Tri
colp
opoll
enit
es p
arm
ula
rius
Tri
colp
opoll
enit
es h
enri
ci
Tri
colp
opoll
enit
es l
ibla
rensi
sli
bla
rensi
sss
p.T
rico
lpopoll
enit
es l
ibla
rensi
sfa
llax
ssp.
Tri
colp
opoll
enit
es a
sper
Tri
colp
oro
poll
enit
es p
seudoci
ngulu
mT
rico
lporo
poll
enit
es c
ingulu
movi
form
isss
p.T
rico
lporo
poll
enit
es c
ingulu
mfu
sus
ssp.
Tri
colp
oro
poll
enit
es c
ingulu
mpusi
llus
ssp.
Tri
colp
oro
poll
enit
es m
arc
odure
nsi
s
Tri
colp
oro
po
llen
ites
meg
aex
act
us
brü
hle
nsi
sss
p.T
rico
lpo
rop
oll
enit
es e
dm
un
di
Tri
colp
oro
po
llen
ites
mic
rore
ticu
latu
s
Tri
colp
oro
po
llen
ites
ole
oid
es
Tri
colp
oro
po
llen
ites
vil
len
sis
Tri
colp
oro
po
llen
ites
so
lé d
e p
ort
ai
Tri
colp
oro
po
llen
ites
kru
sch
ip
seu
do
laes
us
ssp.
Psi
latr
ico
lpo
rite
s cr
ass
us
Tet
raco
lporo
poll
enit
es o
bsc
uru
s
Cord
osp
haer
idiu
msp
.U
ndif
fere
ntia
ted
dino
flag
ella
te c
ysts
Epo
ch
Per
iod
EO
CE
NE
PAL
EO
GE
NE
MID
DL
EL
AT
E
Epo
ch
Per
iod
PAL
EO
GE
NE
EO
CE
NE
Not to scale
not to scale
Pli
cato
poll
is p
lica
tus
Cle
isto
sphaer
idiu
msp
.
Tab
le 6
. O
ccu
rren
ce o
f p
alyn
om
orp
hs
and
ben
thic
fo
ram
inif
era
in t
he
Var
sak
yayl
a F
orm
atio
n. S
ee fi
gu
re 5
fo
r sa
mp
le l
oca
tio
n.
MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY
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
massive beddingflat bedding
fine conglomerate
coarse sandstone
coarsening upward
covered
hematite concretions
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.
MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY
358
Table 7. Description and environmental interpretation for the lithofacies in the Kayıköy Formation.
Facies Description Interpretation
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
concentration turbidity
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-
concentration turbidity
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.
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
MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY
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
massive beddingflat bedding
plant debris
hematite concretions
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.
MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY
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.
MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY
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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MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY
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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)
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1
2
3
4
5
67
9
8
MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY
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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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1 2 3
7
6
8
9
54
MIDDLE−UPPER EOCENE FORMATIONS IN SW TURKEY
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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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7
1
4
2
6
5
3
800μm
200μm350μm
00
0