-
Stratigraphy and Larger Foraminifera of the EoceneShallow-marine
and Olistostromal Units of the Southern
Part of the Thrace Basin, NW Turkey
ERCAN ÖZCAN1, GYÖRGY LESS2, ARAL I. OKAY3, MÁRIA
BÁLDI-BEKE4,KATALIN KOLLÁNYI4 & İ. ÖMER YILMAZ5
1 İstanbul Technical University, Faculty of Mines, Department of
Geology, Maslak, TR−34469 İstanbul, Turkey(E-mail:
[email protected])
2 University of Miskolc, Department of Geology and Mineral
Resources, H−3515 Miskolc-Egyetemváros, Hungary3 İstanbul Technical
University, Eurasia Institute of Earth Sciences, Maslak, TR−34469
İstanbul, Turkey
4 Geological Institute of Hungary H-1143, Budapest, Stefánia út
14, Hungary5 Middle East Technical University, Department of
Geological Engineering, TR−06531 Ankara, Turkey
Received 03 February 2009; revised typescript receipt 10 April
2009; accepted 10 April 2009
Abstract: The Eocene marine sequence in the southern part of the
Thrace Basin (NW Turkey) involves a variety ofplatform and
deep-marine olistostromal units, the stratigraphy of which have
been vigorously debated in the past. Adetailed analysis of larger
foraminifera in these either foraminifera or
foraminifera-coral-coralline algae-dominatedplatform and associated
comparatively deeper-marine units permits us to establish a
high-resolution biostratigraphy inthe context of shallow benthic
zonation (with SBZ zones) of Tethyan Paleogene. The oldest zone
(SBZ 5, correspondingto the basal Ypresian) was observed only in
olistoliths. An old erosional remnant of a transgressive
shallow-marine tobasinal sequence (Dişbudak series; late Ypresian−?
middle Eocene) was recognized below the regionally mostwidespread
carbonate platform unit, the Soğucak Formation. The Dişbudak
sequence, previously considered to belongto the Soğucak Formation
and formally introduced recently, contains larger foraminifera,
such as orthophragmines,nummulitids and alveolinids in its
shallow-marine package referred to SBZ 10 (late Ypresian). The
Soğucak Formation,which often exhibits patch reef developments,
contains a rich and diverse assemblage of
orthophragmines(Discocyclina, Orbitoclypeus and Asterocyclina),
nummulitids (reticulate and other Nummulites, Assilina,
Operculina,Heterostegina and Spiroclypeus), and other benthic taxa
(Silvestriella, Pellatispira, Chapmanina, Orbitolina,
Linderina,Gyroidinella, Fabiania, Halkyardia, Eoannularia,
Sphaerogypsina, Asterigerina, Planorbulina and Peneroplis).
Theirassemblages, referred to SBZ 15/16, 17, 18, 19 and 20 Zones,
provide a precise tool for recording the history of marineevents
which resulted in the deposition of the Soğucak Formation during
four main periods. Their spatial distribution,recorded as late
Lutetian, early Bartonian, late Bartonian and Priabonian, suggests
a marine transgression from WSWto ENE. The Çengelli flysch sequence
overlying the Soğucak Formation in a limited area to the east of
the GeliboluPeninsula, contains benthic foraminifera, mainly from
limestone olistoliths mostly derived from the SoğucakFormation, and
also in the turbiditic strata. The assemblages in the olistoliths
reveal the existence of various shallowmarine limestone sequences
ranging in age from late Bartonian to early Priabonian.
Key Words: southern Thrace, benthic foraminifera, biometry,
taxonomy, biostratigraphy
Trakya Havzası Güneyi Eosen Sığ-Denizel ve Olistostromal
BirimlerininStratigrafisi ve Bentik Foraminiferleri (KB
Türkiye)
Özet: Trakya Havzası (KB Türkiye) güneyindeki denizel Eosen
birimleri stratigrafik konumları tartışmalı platform
vederin-denizel türbiditik ve olistostromal istifleri ile temsil
edilir. Havzanın güneyinde, foraminifer ve/veya
foraminifer-mercan-kırmızı alg bakımından zengin birimlerde
yaptığımız çalışmalar ilk kez bu birimler için yüksek
çözünürlübiyostratigrafik bir sistemin oluşturulmasına imkan
sağlamıştır. Paleontolojik veriler ve arazi gözlemleri
ışığındastratigrafik olarak Soğucak Formasyonu’nun altında daha
önce Trakya’da tanımlanmamış erken Geç İpreziyen−? Orta
27
Turkish Journal of Earth Sciences (Turkish J. Earth Sci.), Vol.
19, 2010, pp. 27–77. Copyright ©TÜBİTAKdoi:10.3906/yer-0902-11
First published online 09 October 2009
-
Eosen yaşlı sığ- ve derin-denizel bir istifin, Dişbudak istifi,
varlığı ortaya konmuştur. Önceki çalışmalarda SoğucakFormasyonu
içinde değerlendirilen, bu birimin sığ-denizel kısmı SBZ 10’u
(erken Geç İpreziyen) temsil edenorthophragmines, nummulitid ve
alveolinid grupları içerir. Yama resifi düzeylerinin yaygın olarak
gözlendiği SoğucakFormasyonu orthophragmines (Discocyclina,
Orbitoclypeus ve Asterocyclina), nummulitid (retikule ve
diğerNummulites grupları, Assilina, Operculina, Heterostegina ve
Spiroclypeus) ve diğer bentik foraminifer grupları(Silvestriella,
Pellatispira, Chapmanina, Orbitolina, Linderina, Gyroidinella,
Fabiania, Halkyardia, Eoannularia,Sphaerogypsina, Asterigerina,
Planorbulina ve Peneroplis) içerir. SBZ 15/16, 17, 18, 19 ve 20 sığ
bentik zonları temsileden bu topluluklar birimin çökelimi ile
ilgili denizel olayların kronolojisinin oluşturulmasını sağlamış
olup dörtönemli dönem; Geç Lütesiyen, Erken Bartoniyen, Geç
Bartoniyen ve Priaboniyen transgresyon dönemleri ortayakonmuştur.
Çengelli fliş istifinin yaygın kireçtaşı olistolitleri (çoğunluğu
Soğucak Formasyonu’ndan aktarılma) vekısmen türbiditik
seviyelerinde ise (geç) Bartoniyen ve Priaboniyen grupları
tanımlanmıştır.
Anahtar Sözcükler: güney Trakya, bentik foraminifer, biyometri,
taksonomi, biyostratigrafi
28
EOCENE FORAMINIFERA OF THE THRACE BASIN
IntroductionEocene units, represented mainly by
platformcarbonates and a flysch sequence containingolistoliths of
varying dimensions, can be traced indiscontinuous outcrops across
the southern part ofthe Thrace Basin (Figures 1−3). In previous
studies,the Eocene platform units were recognized at
twostratigraphic levels. The stratigraphically older one,the
Başaoğlu carbonates of the Karaağaç Formation,crops out in a single
locality in the northern part ofthe Gelibolu Peninsula. The younger
and regionallymore widespread Soğucak Formation is
traceablethroughout the Thrace Basin (Saner 1985; Önal1986;
Sümengen & Terlemez 1991; Siyako & Huvaz2007) (Figure 4).
In this study, we have recognisedanother shallow marine
transgressive sequencebelow the Soğucak Formation north-east of
Şarköynear Doluca Hill. This unit, named the Dişbudakseries by Okay
et al. (2010), is a carbonate-clasticsequence and is quite
different from the carbonateblocks of the Çengelli Formation and
lithologies ofthe Soğucak Formation in containing a
substantialproportion of clastics. The upper part of thesequence is
represented by basinal fine clasticscontaining a badly preserved
pelagic fauna and flora.The Çengelli Formation has not been
differentiatedand mapped in previous studies and was treated aspart
of the Soğucak Formation (Şentürk et al. 1998b)before Okay et al.
(2010) provided a detailed mapand description of the unit.
The Soğucak Formation is a widely recognizedforaminifera- and
coral-dominated platform unitand, owing to its well-developed
patchy reefs, is a
potential reservoir throughout Thrace (Siyako et al.1989; Siyako
& Huvaz 2007). Despite its economicpotential, a complex
biostratigraphic study andinformation about the correlation of its
isolatedsurface outcrops are completely missing. Moststudies were
concerned with faunal assemblages inlocal sections and were far
from revealing a basinscale evaluation. Widespread shallow
marinelimestone outcrops of the Soğucak Formationaround Şarköy
(Doluca Hill) (Figure 3) werepreviously considered either to
represent theSoğucak Formation, or were regarded as olistoliths
inthe Çengelli Formation (Saner 1985; Okay & Tansel1992; Özcan
et al. 2007a). Recently, Okay et al.(2010) have shown that both in
situ SoğucakFormation (Doluca Hill sequence) and
limestonesrepresenting the blocks of the Çengelli Formationoccur in
the same region. The relationship of theselimestone outcrops with
the surrounding clasticrocks cannot be judged with certainty in all
casesmainly due to Miocene cover or tectoniccomplications. Previous
views considering therelationship between the olistostromal unit
and thelimestone outcrops are discussed in Okay et al.(2010).
The olistostromal unit, the Çengelli Formation,formerly
investigated under differentlithostratigraphic names such as the
Korudağ(Sümengen & Terlemez 1991; Şentürk et al. 1998b),Ceylan
(Siyako 2006) or Çengelli Formation (Okay etal. 2010), is made up
of turbidite beds with arhythmic alternation of sandstone and shale
anddebris flow horizons and olistostromes. Clasts in themass flows
mainly include serpentinite and
-
MEC
TAYBESN
10 km
Çanakkale
Mecidiye
SAROS BAY
Çanakk
ale str
ait
Gelibo
lu Peni
nsula
Biga Peninsula
Gelibolu
B
Tayfur
Beşyol
SAZ
Aegean Sea
Lapseki
Bolayır
Marmara Sea
Çanakkale
İstanbulMecidiye
Greece
A
Aegean Sea
Thrace BasinPIR
Pırnar KorudağSample CEL.13
Çeltik
Gökçeada
GİZ.A
GİZ.B
N5 km
C
4 5
1 2 3
6 7 8 9
Gökçeada
Figure 1. Geological map of the Gelibolu Peninsula (B) and
Gökçeada (C) in the southern part of the Thrace Basin(A) and
location of stratigraphic sections. Geological maps simplified from
Temel & Çiftci (2002),Türkecan & Yurtsever (2002) and
Siyako & Huvaz (2007). 1− Ophiolitic units, 2− Lört Limestone,
3−Karaağaç Formation, 4− Fıçıtepe Formation, 5− Soğucak Formation,
6− Keşan and/or Ceylan formations,7− undifferentiated Miocene and
younger units (partly include Oligocene), 8− volcanics, 9−
alluvium.
29
E. ÖZCAN ET AL.
-
18
Şarköy
78
Kızılcaterzi
KocaaliŞenköy
Şarköyreservoir
Sarıkaya T.
Gölcük
Ortaköy-1
Yeniköy
Sofuköy
Çokal
Yüllüce
Al
Al
Al
Tm
Tm
Tm
Teç
Tek
Tek
Tek
Tm
Tm
0 4 km2
N
Marmara Sea
24
14
28
55
35 51
85
29
45
80
82
62
32
3544 22
31
14
1418
20
85
55
2023
23
04
06
40
54
40
28
1825
Şarköy-1
s
s
s
p
bl
Teç
s
lp
g
g
Quaternary alluviumAl
Miocene sandstone, conglomerate
Keşan Fm. - sandstone, shaleEocene
UpperEocene(Priabonian)
sandstone, shale, massflows, olistostromes:s, serpentinite;l,
Eocenelimestone; p, pelagiclimestone; g, granitoid;gb, gabbro
Tm
Teklimestone
serpentinite, metadiabaseblueschist, granitoid
sbedding horizontal bedding overturned bedding
stratigraphic contact
strike-slip fault
bl
gb
gb
77
Ku
So
gn
t r.
34
27°00'00'' 27°07'30''
40°37'30''
27°00'00''
transpressive fault hydrocarbon exploration well
SoğucakLimestone
YEN7-9
SAR 2007BYEN1-4
SAR.4
YEN10
TEKE
202
172
183
2B
649
Şarköy
Mürefte
Marmara Sea
Saros Bay
616
SAR.17
Cinbasarkale H.
Figure 2. Geological map of the region north and west of Şarköy
and location of samples and stratigraphic sections(small boxes).
Geological map from Okay et al. (2010).
30
EOCENE FORAMINIFERA OF THE THRACE BASIN
-
Figure 3. Geological map of the Doluca Hill region northwest of
Mürefte and location of samples and stratigraphic sections(small
boxes). Geological map from Okay et al. (2010).
MürefteAl
A. Kalamış85
Gölcük
Al
Şarköy
Marmara Sea
0 4 km2
N
DolucaHill
66
2410
Mursallı
Yaya
58
38
Tek
Tek
Tm
Tm
Tm
Tm
18
55
Araplı
Tepeköy
Y. Kalamış
Çınarlı
Kirazlı
Çengelli25
29
13
24
18
14
14 5040
Eriklice
Quaternary alluviumAl
Miocene sandstone,conglomerate
Keşan Formationsandstone, shaleEocene
UpperEocene(Priabonian)
LowerEocene
Tek
Tm
Gedik
yol
Teç
s
sandstone, shale, mass flows,olistoliths: s, serpentinite;l,
Eocene limestone; p, pelagiclimestone; gb, gabbro
18
31
35
18
3228
2332
18
26
12
19
s
Çengelli stream
gb
Çengelli Formation
Soğucak Formation
Dışbudak Series
Yörgüç
27°15'00''
40°37'30''
27°07'30''
CEN 2, 428,564
DeveHill
bedding
stratigraphic contactstrike-slip fault transtensional fault
1900, 1901
1907
1902
Tes
Ted
Ganos F
ault
Özcan 2007aet al.
DOL1-2MÜF-B
MÜF-C
MÜF-A
638
ŞAR10-13
31
E. ÖZCAN ET AL.
-
Lutetian
Ypresian
lowerBartonian
upperBartonian
lowerPriabonian
upperPriabonian
lowerOligocene
Gökçeada North of Saros Bay Tayfur Doluca Hill Teke
?
?
?
?
A
B
DE
C
F
G
I
H
J
K
Özcan et al. 2007a
Lört Limestone
Karaağaç Fm. / Başaoğlu member
Dişbudak series
Fıçıtepe Fm.
Soğucak Fm.
Keşan/ Ceylan/Mezardere fms.
Çengelli Fm.
ophiolitic melangemetamorphics
non-deposition orerosion
?
?
Figure 4. Stratigraphic relations of shallow marine Eocene units
in the southern Thrace Basin based on the present study.
Barsindicate the stratigraphic intervals of the studied
sections/samples; A− SAZ (Sazlimanı), B− MÜF (Mürefte) A, C−GİZ
(Gizliliman) A and B, D− TAY (Tayfur), E− BEŞ (Beşyol), F− TEKE
(Teke Hill), G−MÜF (Mürefte) B, H− PIR(Pırnar), I− MEC (Mecidiye),
J− MÜF (Mürefte) C and YEN (Yeniköy), K− ÇEL (Çeltik). The Lower
Priabonian partof the Soğucak Formation studied earlier near Doluca
Hill by Özcan et al. (2007a) is shown by an arrow.
32
EOCENE FORAMINIFERA OF THE THRACE BASIN
foraminifera- and coral-dominated limestone (Okayet al. 2010).
Larger foraminifera occur both in thelimestone blocks and in the
turbiditic sandstones.
This study is part of the revision of largerforaminifera in the
Paleogene shallow marine units
in the Thrace Basin. We present here our data fromEocene
shallow-marine and associated turbiditic andolistostromal units
exposed in the southern part ofthe Thrace Basin. The description of
largerforaminifera and their biostratigraphy from the
-
33
E. ÖZCAN ET AL.
northern and eastern part of the basin is given in asubsequent
paper (Less et al. in review). Theforaminiferal information on
these units is eithercompletely lacking as in the Dişbudak series
andÇengelli Formation, or is very poor and includesdeterminations
usually at generic level, thus notpermitting a high-resolution
biostratigraphicframework (Sümengen & Terlemez 1991;
Çağlayan& Yurtsever 1998; Şentürk et al. 1998a, b) for
theSoğucak Formation. Among these foraminifera,nummulitids
(Nummulites, Heterostegina andSpiroclypeus) and some
orthophragminid taxa areparticularly important since their
recently-proposedevolutionary features allow us to subdivide
somemiddle to late Eocene shallow benthic foraminiferalzones into
sub-zones (Özcan et al. 2007a; Less et al.2008; Less & Özcan
2008). Description of most of thetaxa is based on the study of
isolated specimens ofthe above groups recovered from some
argillaceouscarbonate levels and from thin-sections.
Figured specimens prefixed by ‘O/’ are stored inthe Özcan
collection of the Department of Geology,İstanbul Technical
University, while those marked by‘E.’ are in the Eocene collection
of the GeologicalInstitute of Hungary (Budapest).
Abbreviations for biozones: NP− Paleogenecalcareous
nannoplankton zones by Martini (1971);OZ− Orthophragminid zones for
the MediterraneanPaleocene and Eocene (Less 1998a) with
correlationto the SBZ zones; P− Paleogene plankticforaminiferal
zones by Blow (1969), updated byBerggren et al. (1995); SBZ−
shallow benthicforaminiferal zones for the Tethyan Paleocene
andEocene (Serra-Kiel et al. 1998, with additional sub-zones for
SBZ 18 and 19 by Less et al. 2008) withcorrelations to the
planktonic and magnetic polarityzones. The correlation of these
zonations is shown inFigure 5.
Stratigraphy and Palaeontological Background ofthe
Shallow-marine and Olistostromal EoceneUnits in the Southern
ThraceThe most complete Eocene sequence in southernThrace Basin
crops out in the northern part ofGelibolu Peninsula along the
southern shore of SarosBay (Figure 4). The lowest observable part
of the
sequence includes a deep-marine argillaceouscarbonate unit
containing Late Cretaceous and EarlyPaleocene planktonic
foraminifera (Önal 1986). Thestratigraphic position of this unit,
just exposed in alimited area, is not clear and it is overlain by
asequence of massive deep-marine marls representingthe lower part
of the Karaağaç Formation. Anoutcrop of a 3−5-m-thick shallow
marine carbonatesequence (Başaoğlu member of Karaağaç
Formation)with a limited lateral extent (about 100−150 m)
wasobserved just above the lower marls of the KaraağaçFormation.
This unit, containing a very richassemblage of nummulitidae and
orthophragmines,has been considered to mark an early
Eocenetransgression. The field observations show a sharpcontact
between carbonates and marls below andabove, suggesting that it is
an olistolith in theKaraağaç Formation. The finding of a
smallerolistolith in the same area also supports this view.The age
of Başaoğlu member was considered to beearly Eocene (Önal 1986) and
early−middle Eocene(Temel & Çiftci 2002).
Our knowledge about the faunal composition andchronology of the
transgressive Eocene sequencescomes mainly from the Soğucak
Formation, tracedin continuous and widespread outcrops across
thenorthern part of the Thrace Basin (Konak 2002;Siyako 2006). The
Soğucak Formation can also betraced in discontinuous outcrops in
the southernpart of the basin in the Biga Peninsula (Siyako et
al.1989), in the Gelibolu Peninsula (Önal 1986; Siyakoet al. 1989;
Sümengen & Terlemez 1991; Siyako &Huvaz 2007) and in the
islands of Gökçeada andBozcaada (Temel & Çiftçi 2002; Siyako
& Huvaz2007). It is a platform carbonate unit containing arich
association of benthic foraminifera and otherfossil groups, such as
corals, molluscs, bryozoans,echinoids and coralline red algae (Daci
1951; Keskin1966, 1971; Önal 1986; Şentürk et al. 1998a, b;
Temel& Çiftci 2002). Unlike the lower Eocene unitsdescribed
from Bozcaada in the Aegean Sea (Varol etal. 2007) and the Armutlu
peninsula (Özgörüş et al.2009), patch-reef carbonates constitute a
prominentpart of the platform succession. Our data suggestthat most
shallow marine limestone olistoliths in theÇengelli Formation
originated from this unit.Previous studies on the fossil
composition of the
-
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Figure 5. Correlation of orthophragminid biozones with late
Paleocene and Eocene planktonic foraminiferal,
calcareousnannoplankton and shallow benthic biozones, based on Less
et al. (2007, 2008) and on Özcan et al. (2007a, b),
slightlymodified. Time scale based on Graciansky et al. (1999).
34
EOCENE FORAMINIFERA OF THE THRACE BASIN
Soğucak Formation in the basinal scale reported richand diverse
foraminiferal taxa belonging toNummulites, Discocyclina,
Heterostegina,Spiroclypeus, Operculina, Assilina,
Glomalveolina,Pellatispira, Chapmanina, Linderina,
Silvestriella,Orbitolites, Halkyardia, Gyroidinella,
Fabiania,Eoannularia and Asterigerina (Daci 1951; Önal 1986;Şentürk
et al. 1998a, b). The most comprehensiveand systematic
foraminiferal data from the SoğucakFormation were presented by Daci
(1951), whoassigned a Lutetian−Priabonian age to the unitwidely
exposed west of İstanbul, and by Özcan et al.(2007a), who described
from the Şarköy section(corresponding to the upper part of the
SoğucakFormation from the southern slope of Doluca Hill)an
assemblage of early Priabonian largerforaminifera belonging to
Discocyclina, Nemkovella,Asterocyclina, Orbitoclypeus,
Nummulites,Heterostegina, Spiroclypeus, Assilina and
Operculina.
In most studies the Soğucak Formation wasregarded as of ‘middle’
Eocene age without a highresolution perspective, although different
parts ofthe unit were referred either to the Lutetian, orPriabonian
mainly based on larger foraminifera,molluscs and corals (Keskin
1966, 1971; Önal 1986;Sümengen & Terlemez 1991; İslamoğlu &
Taner1995; Çağlayan & Yurtsever 1998; Şentürk et al.1998a, b;
Temel & Çiftci 2002; Siyako & Huvaz 2007).A transgressive
shallow marine successioncontaining Ypresian alveolinids and
nummulitidshas lately been considered to represent the
SoğucakFormation on Bozcaada island by Varol et al. (2007).We
believe that this marks a much older marinetransgression and that
the Alveolina-dominated‘Soğucak’ Formation of the authors cannot
becorrelated with the coral-foraminiferal-algalSoğucak Formation
marking a younger inundation
event in Thrace. Our data suggest that the unitdescribed from
this island may be comparable withthe Dişbudak series of Okay et
al. (2010).
The larger foraminiferal composition of theolistostromal unit,
the Çengelli Formation, is notknown. In most previous studies, the
age of the unit(commonly referred to as the Ceylan or
KorudağFormation) was reported to be late Eocene(Sümengen &
Terlemez 1991; Toker & Erkan 1984)or late Eocene−early
Oligocene (Çağlayan &Yurtsever 1998). These ages were obtained
fromcorrelative units in southern or northern Thrace. Inthe study
area larger foraminifera occur either inturbiditic levels or in the
limestone olistoliths of theÇengelli Formation. Okay & Tansel
(1992) describedsome pelagic limestone blocks containing bothupper
Cretaceous and Paleocene planktonicforaminifera.
Description of the Eocene Shallow-marine andOlistostromal Units
and Their PalaeontologicalContentBaşaoğlu Member of Karaağaç
FormationSection SAZ (Sazlimanı). This is a limestone unitabout 5 m
thick exposed only between Saz Limanıand Karaağaç, north of Tayfur
village (Section SAZ,UTM coordinates: 0452324, 4475992, Figure 1B).
Itrepresents an olistolith in the late Paleocene−earlyEocene
basinal sequence of the Karaağaç Formationand comprises a rich
assemblage of genusNummulites (undetermined in species level)
andrare orthophragmines. These (identified only insample SAZ 46)
are represented by Discocyclinaseunesi karabuekensis, Nemkovella
stockari,Orbitoclypeus schopeni neumannae, O. munieri cf.
-
ponticus, O. bayani cf. bayani. The first two taxa
arecharacteristic for the OZ 2 Zone while the third onetypifies the
OZ 3 Zone, although biometrically (Table2) it is very close to O.
schopeni ramaraoi, thepylogenetic ancestor, whose range ends in OZ
2.Since Orbitoclypeus bayani bayani also starts in OZ 3,the age of
the above assemblage can be determined asOZ 2-3, corresponding to
the SBZ 4-7 zones.However, since genus Nummulites first appears
onlyin the SBZ 5 Zone, the age of this olistolith is thoughtto
cover the SBZ 5-7 Zones, which corresponds toearly–middle Ilerdian.
Formerly (Serra-Kiel et al.1998) the early Ilerdian was correlated
with the lateThanetian. However, the base of the Ilerdian and ofthe
Ypresian proved to be coeval (Pujalte et al.(2009a, b), and hence
the Sazlimani olistolith is ofearliest Ypresian age.
Dişbudak SequenceSection MÜF (Mürefte) A. The section is a
clastic-carbonate sequence about 30 metres thick, exposeddue east
of Doluca Hill, north-east of Şarköy (SectionMÜF.A, UTM
coordinates: 0517151, 4505041)(Figures 3 & 6). The lowest part
of this highlyfossiliferous rock sequence comprises
conglomeratesand sandstones with a wealth of oysters at its
base.This passes upwards into sandstones withintercalated
conglomerate horizons, that grade intolimy sandstone and/or sandy
limestones containing arich assemblage of Nummulites, Orbitolina
andalveolinids. These levels are almost devoid oforthophragmines
and are interpreted to have beendeposited in an inner shelf
environment. The top ofthe profile (sample MÜF A 10) is
characterized by anodular limestone containing a diverse
assemblageof nummulitids [among which Assilina placentula(Deshayes)
predominates], orthophragmines andvery sporadic tests of corals
(Figure 7) andrepresenting a middle/outer shelf environment.
A10-m-thick siltstone-marl succession was observedto overlie these
nodular limestones although therelation between them is not yet
fully clear. It is mostlikely that these fine clastics record a
deepening inthe depositional environment following thedeposition of
nodular carbonates. Based on theassemblage presented in Figure 7,
the carbonatesuccession is regarded as early late Ypresian
(early
Cuisian) in age (SBZ 10), although the presence of D.archiaci
ex. interc. staroseliensis-archiaci suggests atransitional position
between lower and upperYpresian (SBZ 9 and 10). Two samples (MÜF A
11and 1909) representing the fine clastics overlying thenodular
limestone have been analysed for calcareousnannoplakton and
planktonic foraminifera. SampleMÜF A 11 yielded a calcareous
nannoplanktonassemblage (Figure 7) among which Discoasterlodoensis
has the shortest stratigraphic range (NP 12-14) corresponding to a
late Ypresian−earliestLutetian time span. This sample also
containsreworked Campanian forms, such as
Eiffellithusturriseiffelli, E. eximius, Watznaueria
barnesae,Arkhangelskiella cymbiformis, Broinsonia parca s.
l.,Bukryaster hayi and Cretarhabdus sp. Planktonicforaminifera in
this sample are quite rare and areonly represented by badly
preserved Acarininaprimitiva, which indicates a general
early−middleEocene age. Age data from sample 1909 near DolucaHill
(Figure 3) are controversial. The planktonicforaminiferal
assemblage of Globorotalia bullbrooki,G. cerroazulensis
cerroazulensis, Morozovellaspinulosa, Globigerina eocaena, G.
linaperta, G. senni
MÜF.A1
10
MÜF.B 210
Doluca Hill
MÜF.A 11
upper Bartonian limestone
Figure 6. Overview of the Dişbudak sequence (section Mürefte−
MÜF.A; upper Ypresian) and the overlying SoğucakFormation (section
Mürefte − MÜF.B; upperBartonian) east of Doluca Hill, looking south
from theÇengelli flysch sequence. Limestone lenses denote
thenodular limestone level in MÜF.A and coralline algal-coral
facies in MÜF.B. Sample MÜF A 11 representsthe basinal fine
clastics overlying the upper Ypresiannodular limestone of Dişbudak
sequence in thedownthrown block. Numbers refer to samples.
35
E. ÖZCAN ET AL.
-
8
12 6 5
5 2
9 4
18 m �10
Disc
ocyc
lina
forti
si fo
rtisi
D. a
rchia
ci ex
. inter
c. sta
rose
liens
is-ar
chiac
iD.
arc
hiaci
arch
iaci
D. a
ugus
tae
sour
bete
nsis
D. d
ispan
sa t
auric
aNe
mko
vella
stro
phiol
ata
indet.
ssp.
N. e
vae
indet.
ssp.
Orbit
oclyp
eus
douv
illeic
f. dou
villei
O. sc
hope
ni ind
et. ss
p.As
tero
cycli
na st
ella
indet.
ssp.
Num
muli
tes l
eupo
ldiN.
bur
digale
nsis
N. n
emko
viN.
soer
enbe
rgen
sisNu
mm
ulite
ssp.
Assil
ina p
lacen
tula
Assil
inasp
.Al
veoli
nasp
.Or
bitoli
tess
p.Ro
talid
foram
inifer
a
Ortho
phra
gmine
sMi
liolid
sTe
xtular
idsBr
yozo
ans
Cora
lsGa
strop
ods
Echin
odids
Biva
lves
Disc
olith
ina m
ultipo
raCy
clica
rgoli
thus
florid
anus
Cocc
olith
us p
elagic
usCy
clico
ccoli
thus
form
osus
Disc
oaste
r lod
oens
isSp
heno
lithus
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ns
10
SBZ
SECTION MÜF.A & SAMPLE 1894
2.5 1
STAG
Elow
er up
per Y
PRES
IAN
7
3
15 9
Nummulites Orthophragmines CoralsGastropodsAssilina
Alveolinidae
sample 1894
NP
11
12-1
3/ 14
10luY
Oysters
Figure 7. Distribution of benthic foraminifera and other fossil
groups in section MÜF (Mürefte) A and sample 1894(Dişbudak
sequence). luY− lower upper Ypresian.
36
EOCENE FORAMINIFERA OF THE THRACE BASIN
and Heterolepa dutemplei is characteristic (based onthe
appearance of muricate Globorotalia) of the earlymiddle Eocene (P
10-12) or, less probably, theyoungest (P 9) Ypresian zone.
Meanwhile thecalcareous nannoplankton (Coccolithus
pelagicus,Cruciplacolithus tenuis, Chiasmolithus sp.,Zygrhablithus
bijugatus, Discoaster multiradiatus, D.binodosus, D. barbadiensis,
Sphenolithus moriformis)indicate the NP 9-10 zones around
thePaleocene/Eocene boundary. This sample alsocontains reworked
Cretaceous forms such asZeugrhabdotus embergeri, Eiffellithus
turriseiffeli,Cribrosphaerella ehrenbergii, Watznaueria
barnesae,Arkhangelskiella cymbiformis and Microrhabdulus sp.In view
of the much younger age given by planktonicforaminifera we think
that all the nannoflora ofsample 1909 is reworked.
Sample 1894. A spot sample was collected from theshallow marine
part of the Dişbudak seriesimmediately east of Doluca Hill (Sample
1894, UTMcoordinates: 0516027, 4504475) (Figure 3). It
alsoconsisted of argillaceous carbonates and containedalmost the
same assemblage of nummulitids (withthe same predominance of
Assilina placentula) andorthophragmines as sample MÜF A 10, but
alsoincluded Discocyclina archiaci archiaci (Figure 7),indicating
an early late Ypresian (early Cuisian) age(SBZ 10 Zone).
Soğucak FormationExposures of the Soğucak Formation can
beobserved around Gökçeada, Gelibolu Peninsula(Tayfur, Beşyol
villages and around Tepe Hill atSarıkaya Sliver), Şarköy (Doluca
Hill) and north of
-
Saros Bay (Pırnar and Mecidiye villages) (Figures1−3).
Gökçeada Island (sections GİZ.A and GİZ.B). TheSoğucak Formation
only crops out in a limited areawest of Gökçeada. Two sections,
GİZ.A (UTMcoordinates: 0386973, 4442620; 0387037, 4442588,Figure
1C) and GİZ.B (UTM coordinates: 0387448,4443239; 0387011, 4442533,
Figure 1C) weresampled near Gizliliman. The lower part of a
47-m-thick section of carbonates in the stratigraphicallylower
section, GİZ.B, is represented below bycoralline red algae and
coral-dominated strata, andby foraminifera and coralline
algae-dominatedhorizons at higher levels. Nummulitids occur only
inthe upper part of the section. The distribution offoraminifera
and other fauna and flora is shown inFigure 8. With the absence of
diagnostic Bartonianforms, such as O. ex. gr. gomezi and
reticulateNummulites, and its position below the well-described
Bartonian part in section GİZ.A, thissection is considered to be of
late Lutetian age (SBZ15-16). Section GİZ.A stratigraphically
overlyingsection GİZ.B is represented by a 66-m-thicksequence of
limy siltstones, sandstones andlimestone beds with abundant larger
foraminiferaand represents a more distal depositional settingthan
section GİZ.B. Foraminifera are abundant anddiverse at numerous
levels. Corals are sporadic andtransported. These carbonates are
overlain by pelagicmarls, but their relationships were not
observedbecause of a fault between the carbonates andoverlying
marls (Figure 1C). The lower part of thesection (samples GİZ A 4-8)
is regarded to be of lateLutetian (SBZ 15-16) age, based on the
assemblage(Figure 9), containing Discocyclina prattimontfortensis,
Asterocyclina stellata adourensis andlacking Operculina ex. gr.
gomezi. The upper part(samples GİZ A 9-14) of the section is
assigned anearly Bartonian (SBZ 17) age, based on the
firstoccurrence of O. ex. gr. gomezi and the presence
ofcharacteristic Bartonian taxa such as Orbitoclypeusdouvillei
malatyaensis and O. haynesi. The basinalmarls of the Ceylan
Formation are very rich incalcareous nannoplankton and
planktonicforaminifera. A sample (GİZ B 15; UTM coordinates0388056,
4442442) collected close to section GİZ.B
(but separated very probably by a fault from theplatform
carbonates) yielded a calcareousnannoplankton assemblage of
Discolithinamultipora, Isthmolithus recurvus,
Cyclicargolithusfloridanus, Reticulofenestra placomorpha, R.
bisecta,Chiasmolithus oamaruensis, Coccolithus
pelagicus,Cyclococcolithus formosus, Discoaster sp.,Sphenolithus
moriformis and S. predistentus. Thecoexistence of Chiasmolithus
oamaruensis,Isthmolithus recurvus and Cyclococcolithus
formosussuggests a late Eocene (NP 19-20, Priabonian) age forthis
sample. The same sample yielded a planktonicforaminiferal
assemblage of Globigerinacryptomphala, Globigerina eocaena,
andGlobigerinatheka index tropicalis, suggesting itprobably belongs
to the lower Upper EoceneGlobigerinatheka semiinvoluta (P 15)
Zone.
Section TAY (Tayfur). This is a clastic-carbonatesequence about
15 metres thick, exposed due southof Tayfur (Section TAY, UTM
coordinates: 0455404,4472526) (Figure 1B). The section is
represented byalgae and foraminifera (mainly
nummulitids,alveolinids and orthophragmines)-dominated
GİZLİLİMAN (GİZ.B)
SO
ĞU
CA
K F
OR
MAT
ION
upp
er L
utet
ian
15-1
6
N. ex
. gr. p
erfo
ratu
s Nu
mm
ulite
s sp.
Gyro
idine
lla m
agna
Fabia
nia ca
ssis
Aste
riger
ina ro
tula
Spha
erog
ypsin
a glo
bula
Linde
rina
sp.
Gyps
ina sp
.ro
talid
foram
inifer
aOr
thoph
ragm
ines
Alve
olinid
sMi
liolid
sTe
xtular
idsBr
yozo
ans
Cora
lline r
ed al
gae
Cora
lsCr
inoids
Biva
lves
47 m 1945 1843 17
36 1433 13
27 11
19 8
39 16
18 7
13 510 46 32 20 1
10
38 15
6
9
30 12
?
? ?
FIÇ
ITE
PE
SBZ
STAG
E
UNIT
Figure 8. Distribution of benthic foraminifera and other
fossilgroups in section GİZ (Gizliliman) B (SoğucakFormation).
37
E. ÖZCAN ET AL.
-
GİZLİLİMAN (GİZ.A) S
OĞ
UC
AK
FO
RM
ATIO
N lo
wer B
arton
ian17
5.5 �3
1.9 �1
21 5
2.3 2
8.5 �4
24.5 �629.5 �733 �8
39 �942 �1044.8 �1152 �1260.7 �1366 m 14
Disc
ocyc
lina
augu
stae
atlan
tica
D. d
ispan
sa se
llaD.
disc
usD.
nan
dori
D. p
ratti
mon
tforte
nsis
Orbit
oclyp
eus v
arian
s rob
erti
O. h
ayne
siO.
dou
villei
cf. p
anno
nicus
O. d
. mala
tyaen
sisAs
tero
cycli
na st
ellat
a ste
llata
A. st
ellat
a ad
oure
nsis
A. k
ecsk
emet
iiNu
mm
ulite
s ex.
gr. m
illeca
put
N.ex
. gr. p
erfo
ratu
s Nu
mm
ulite
sspp
.As
silina
ex. g
r. alpi
naOp
ercu
lina
ex. g
r. gom
ezi
Spha
erog
ypsin
a glo
bula
Linde
rina
sp.
Gyps
inasp
.Mi
liolid
sBr
yozo
ans
Cora
lline r
ed al
gae
Cora
lsCr
inoids
Biva
lves
15-1
6up
per L
utet
ian
SBZ
STAG
E
UNIT
Figure 9. Distribution of benthic foraminifera and other fossil
groups in section GİZ (Gizliliman) A(Soğucak Formation).
38
EOCENE FORAMINIFERA OF THE THRACE BASIN
carbonate levels of the Soğucak Formation and iscompletely
devoid of corals, suggesting an inner shelfdepositional setting.
These carbonates are in tectoniccontact with the overlying pelagic
marls. Fossilassemblages (Figure 10), including Operculina ex.
gr.gomezi, but lacking the genus Heterostegina, indicatean early
Bartonian (SBZ 17) age. Some other largerforaminiferal components,
such as Nummulitesbiedai, suggest a somewhat younger age, while
others(Orbitoclypeus varians roberti) indicate a slightlyolder age.
In summary, the upper part of the Tayfursection most probably
belongs to the SBZ 17 Zone.
Section BEŞ (Beşyol). This clastic-carbonate sequenceof the
Soğucak and Ceylan Formations, about 88metres thick, is exposed due
east of Beşyol village(Section BEŞ, UTM coordinates: 0445329,
4468144,Figure 1B). The lower part of the Soğucak carbonatesequence
comprises limestones with bivalves,sporadic nummulitids and corals:
their relationshipwith the clastics of the underlying Fıçıtepe
Formation is poorly exposed. The SoğucakFormation is rich in
large Nummulites biedai (sampleBEŞ 8) in the middle and upper parts
of the section.The shallow marine carbonates pass upwards into
afine clastic silty-marly sequence with sandstoneintercalations
containing pelagic fauna and flora.Larger foraminifera occur
abundantly only at thetransition (sample BEŞ 19) between the
carbonatesand the overlying fine clastics. The fine clasticsyielded
a calcareous nannoplankton assemblage ofCyclicargolithus
floridanus, Reticulofenestra bisecta,Coccolithus pelagicus, C.
eopelagicus, Cyclicoccolithusformosus, Braarudosphaera bigelowi,
Pemma sp. andSphenolithus moriformis in sample BEŞ 21,suggesting a
middle Eocene age for this part of thesection. In these beds
planktonic foraminifera arevery scarce. The basinal clastics are
almost devoid ofbenthic foraminifera. The top of the profile
(samplesBEŞ 26 and 27) is characterized by a limestonehorizon
containing a diverse assemblage ofnummulitids and other benthics.
This 3-m-thick
-
limestone horizon is in turn overlain by more basinalclastics
devoid of larger foraminifera. Based on thisassemblage (Figure 11),
the age of the lowercarbonate succession should be similar to that
of theshallow marine part of the Tayfur section (seeabove), i.e. it
belongs to the upper part of the SBZ 17Zone (late early Bartonian).
Heterostegina (cf.armenica) occurs in the upper carbonate
level(sample BEŞ 27) suggesting a late Bartonian age (SBZ18) for
it.
Section Teke. This Soğucak Formation carbonatesuccession
approximately 50 metres thick isinterpreted as resting
unconformably upon theserpentinite of the Sarıkaya sliver (Okay et
al. 2010).An exposure due west of Teke Hill has been sampled(UTM
coordinates: 94978, 91904; 94860, 91959,Figures 2 & 12). The
distribution of largerforaminifera (their richest assemblage can be
foundin sample TEKE 6) and other fossil groups is shown
in Figure 13. The abundant occurrence ofPlanorbulina, not
recorded in Bartonian blocks inthe study area, in the lower to
middle parts ofsequence, is noteworthy. This part of the
carbonatesalso contains miliolids, bryozoans, echinoids,
corals,bivalves and coralline algae. The foraminiferalassemblage
(mainly based on the occurrence ofHeterostegina reticulata
mossanensis, Spiroclypeussirottii and Nummulites fabianii)
confidentlyindicates the SBZ 19A Sub-zone, and implies anearliest
Priabonian age for the Soğucak Formation.
Section MÜF (Mürefte) B. A 19-metres-thick sectionrepresenting
the basal part of Soğucak Formationwas measured east of Doluca Hill
(MÜF.B, UTMlocation: 0517306, 4505174, Figure 3). This locality
isclose to the Dişbudak series (MÜF.A) (Okay et al.2010). The basal
part of the profile consists of 11-metre-thick limestones (samples
MÜF B 2 to 6)containing an association (Figure 14) in
whichmiliolids are the most common foraminifera. Thisassemblage
indicates an inner shelf depositionalenvironment for the lower part
of the sequence. Theoverlying horizons (samples MÜF B 7-10) contain
amore diverse association with different species ofNummulites. The
single Heterostegina reticulataspecimen in sample MÜF B 9 has about
9 undividedpost-embryonic operculinid chambers, suggestingthat it
may belong to H. r. multifida. Miliolids arerarely identified. The
uppermost part of the sectionis represented by coralline red algae
and corallimestone facies containing mainly tests of
corals,coralline red algae and scarce miliolids. Theaforementioned
associations indicate an inner tomiddle shelf depositional
environment for thecarbonates. The foraminiferal assemblages just
belowthe coral-algal limestone levels can be assigned to theSBZ 18
Zone (late Bartonian), based on the jointoccurrence of Nummulites
biedai, N. hormoensis,highly advanced N. striatus and relatively
primitiveH. reticulata.
Section PIR (Pırnar). This is a 108-metres-thicksection of
carbonates (UTM coordinates: 0470000,4506590; 0469790, 4506743,
Figure 1B) from theSoğucak Formation and overlying deep-marine
units
TAYFUR (TAY)
SO
ĞU
CA
K F
M.
low
er B
arto
nian
17
�3
0 �1 2
�415 m �5
Disc
ocyc
lina
dispa
nsa
cf. d
ispan
saOr
bitoc
lypeu
s var
ians r
ober
tiO.
zitte
li Nu
mm
ulite
s bied
ai Nu
mm
ulite
ssp.
Oper
culin
aex
. gr. g
omez
iMi
liolid
s
F. F
M.
??C.
FM.
SBZ
STAG
EUN
IT
Figure 10. Distribution of benthic foraminifera and other
fossilgroups in section TAY (Tayfur, Soğucak Formation).
39
E. ÖZCAN ET AL.
-
BEŞYOL (BEŞ)
Orbit
oclyp
eus z
itteli
O. va
rians
ex. in
terc.
robe
rti-s
calar
isAs
tero
cycli
na st
ellat
aA.
kecs
kem
etii
Num
muli
tes b
iedai
Num
muli
tess
p.Op
ercu
lina
ex. g
r. gom
ezi
Gyro
idine
lla m
agna
Fabia
nia ca
ssis
Aste
riger
ina ro
tula
Spha
erog
ypsin
a glo
bula
Calca
rina
sp.
Orbit
olite
ssp.
Linde
rina
sp.
Hete
roste
gina
sp.
plank
tonic
foram
inifer
aOr
thoph
ragm
ines
Alve
olinid
sMi
liolid
sRo
talid
Fora
minif
era
Textu
larids
Bryo
zoan
sCo
rallin
e red
alga
eCo
rals
Gastr
opod
sEc
hinoid
sCr
inoids
Biva
lves
SO
ĞU
CA
K F
OR
MAT
ION
Bar
toni
an
12.5 �8
88 m 2785 26
53 23
65 2560 24
44 2236 21
20
21.5 1821 17
17.5 1417 1316.5 12
11
14 9
19 16
12 7 6
11 510 48 35 2
23 �19
04 1
16 10
18 15
CE
YLA
N F
M.
1718
17 o
r 18
FIÇI
TEPE
FM.
? ?SB
Z
STAG
E
UNIT
Figure 11. Distribution of benthic foraminifera and other fossil
groups in section BEŞ (Beşyol, SoğucakFormation).
40
EOCENE FORAMINIFERA OF THE THRACE BASIN
(Ceylan/Keşan Formation) exposed close to Pırnarvillage. The
underlying rocks and the lower part ofthe Soğucak Formation are not
exposed in theregion. The shallow-marine carbonate sequence
isrepresented throughout the section by foraminifera,coralline
algae-foraminifera or coralline algae-coraldominated levels (Figure
15). Miliolids are abundantat some levels in the lower and middle
part of the
sequence, whereas coral-dominated limestone levelsmore
frequently occur in the upper levels. Largerforaminifera (except
for the uppermost levels, wherethey are the main biogenic
contributors) occur onlyat certain horizons and are mainly
represented byNummulites. This part of the section is interpreted
tohave been deposited in an inner to middle shelfenvironment. The
uppermost part of the section
-
contains more clastic material and largerforaminifera in
rock-forming abundance at somelevels. Orthophragmines are more
abundant in thispart of the section and are accompanied mostly
bynummulitids, suggesting more distal platformconditions than the
lower part of the section. Basedon its assemblage (Figure 15), most
of the carbonatesuccession is regarded as late Bartonian in
age,although the lower part of the section with nomarker forms may
still be early Bartonian. The
evolution of the Heterostegina armenica lineage, amarker taxon
for the early and middle lateBartonian, is nicely observed in the
upper part of thesection. Based on these, most of the sequence with
H.armenica armenica but lacking H. reticulata can beassigned to an
early late Bartonian age (SBZ 18A).The uppermost part of the
carbonates, containing H.armenica tigrisensis and H. reticulata cf.
tronensis,can already be attributed to the middle lateBartonian
(SBZ 18B). Nummulites lyelli with largetests of B-forms also occurs
here.
The carbonate levels pass up into pelagic marls ofthe
Ceylan/Keşan Formation. A sample (PIR 48A)from the lowest part of
these basinal clastics containsa calcareous nannoplankton
assemblage ofCyclicargolithus floridanus, Reticulofenestra
bisecta,R. cf. placomorpha, Coccolithus pelagicus,Cyclococcolithus
formosus, ?Lanternithus minutus,Braarudosphaera bigelowi,
Discoaster barbadiensis,D. cf. tani, Sphenolithus moriformis and S.
radians,suggesting a middle Eocene age (NP 16-17).
TEKE 6TEKE 10
Figure 12. Overview of the section TEKE (lower Priabonian)from
the transgressive Soğucak Formation west ofTeke Hill. The locations
of two samples are shown.
7
50 m 10
5
3 2
9
Disc
ocyc
lina
prat
ti pra
ttiAs
tero
cycli
na a
. cf. d
anub
icaA.
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ata
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risA.
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riabo
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isA.
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etii
Orbit
oclyp
eus v
arian
s sca
laris
O. zi
tteli
Num
muli
tes f
abian
iiSp
irocly
peus
siro
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silina
ex. g
r. alpi
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tero
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a r. m
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isGy
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isAs
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erina
rotu
laSp
haer
ogyp
sina
globu
laNu
mm
ulite
s sp.
Halky
ardia
sp.
Orbit
olite
s sp.
Linde
rina
sp.
Gyps
ina sp
.Pl
anor
bulin
a sp
.
Ortho
phra
gmine
sMi
liolid
sTe
xtular
idsBr
yozo
ans
Cora
lline r
ed al
gae
Cora
lsGa
strop
ods
Echin
oids
Crino
idsBi
valve
s
SOĞ
UC
AK
FM
.
SBZ
19
thick.(app.)
SBZ
SECTION TEKE
lower
PRI
ABON
IAN
�1
�4
�6?
STAG
E
ophiolites
�8
UNIT
Figure 13. Distribution of benthic foraminifera and other fossil
groups in shallow marine carbonates of the SoğucakFormation in
section TEKE (Teke Hill).
41
E. ÖZCAN ET AL.
-
13 �7
19m 10
8
10 6 5
3 30 2
5 4
15 �9
Orbit
oclyp
eus v
arian
s cf. s
calar
is-ro
berti
Num
muli
tes h
orm
oens
isN.
bied
aiN.
stria
tus
Num
muli
tess
p.As
silina
ex. g
r. alpi
naHe
tero
stegin
a re
ticula
ta in
det.s
sp.
Gyro
idine
lla m
agna
Silve
striel
la te
traed
raCh
apm
anina
gas
sinen
sisFa
biania
cass
isEo
annu
laria
eoce
nica
Aste
riger
ina ro
tula
Spha
erog
ypsin
a glo
bula
Halky
ardia
sp.
Orbit
olite
ssp.
Pene
ropli
ssp.
Gyps
inasp
.Ro
talia
sp.
Ortho
phra
gmine
sMi
liolid
sTe
xtular
idsBr
yozo
ans
Cora
lline r
ed al
gae
Dasy
clada
cean
alga
eCo
rals
Gastr
opod
sEc
hinoid
sCr
inoids
Biva
lves
SBZ
18
sample
SBZ
SECTION MÜF.B
STAG
Eup
per
BART
ONIA
N
Nummulites Orthophragmines Heterostegina Corals GastropodsDiş
budaksequence
SOĞU
CAK
FM.
UNIT
Figure 14. Distribution of benthic foraminifera and other fossil
groups in section MÜF.(Mürefte) B (Soğucak Formation).
42
EOCENE FORAMINIFERA OF THE THRACE BASIN
Samples from Mecidiye Region. The most widespreadoutcrops of the
Soğucak Formation north of SarosBay are found around Mecidiye
(Figure 1B). Thisunit unconformably overlies the clastics of
theFıçıtepe Formation, which unconformably rests onmetamorphic
units (Figure 16). The carbonatesuccession is mainly represented by
foraminifera,coralline algae and coral-dominated
limestones,suggesting a variety of depositional settings
betweeninner and outer shelf environments. A set of samplesfrom
these carbonates were collected from itswidespread outcrops near
Mecidiye. The commonestlarger foraminifera are represented
byorthophragmines and heterosteginids (Figure 17).Nummulites are
very sporadic. Two samples, onecollected from the basal part of the
SoğucakFormation (sample MEC 40) and the other (sampleMEC 41) from
the upper part, where the carbonatesgrade into clastics of the
Keşan/Ceylan formation,have yielded free tests of larger
foraminifera. SampleMEC 40 contains Spiroclypeus carpaticus,
adiagnostic late Priabonian (SBZ 20) taxon, although
Heterostegina reticulata is represented by H. r. cf.mossanensis
(based on few specimens), a marker forthe early Priabonian (Figure
17). All samplescollected from the lowest part of the section
justsouth of Mecidiye (samples MEC 15-24) containHeterostegina
gracilis, a good marker for the latePriabonian (SBZ 20) (Figure
23). Thus, even thelower part of the Soğucak Formation belongs to
thelate Priabonian. Sample MEC 41 also contains H.gracilis,
indicating that the upper part of the unit isalso of late
Priabonian age.
Samples from Doluca Tepe (Şarköy). The outcrops ofthe Soğucak
Formation are widely seen aroundDoluca Hill, north of Şarköy
(Figure 3). AlthoughÖzcan et al. (2007a) interpreted this large
limestonebody as a huge olistolith, it has since beenreinterpreted
as an in situ deposit (Okay et al. 2010)of the Soğucak Formation,
transgressively overlyingthe lower (−middle) Eocene Dişbudak
series. Thetopmost part of this limestone (samples ŞAR 2, 4
&
-
0 1
12 �10
PIRNAR (PIR)
72 37
59 3158 3054 29
52 2748 2645 2541 2437 23 2236 20
28 1825 17
18 1416 1315 12
11
11 9
21 16
8 88 77 66 54 41 3 2
�15
�21
�28
61 32
3564 34
77 4075 3973 38
�33
�36
104 49
93 47
85 44
84 4279 41
�43
90 �4591 �46
99 �48
108 50
?
?
?
�41A
�47A
48ADi
scoc
yclin
a au
gusta
eD.
aug
usta
e oli
anae
D. a
ugus
tae
olian
ae-a
ugus
tae
D. d
ispan
sa d
ispan
saD.
radia
ns in
det s
sp.
D. ra
dians
cf. la
batla
nsis
D. tr
abay
ensis
Orbit
oclyp
eus v
arian
s sca
laris
O. zi
tteli
Aste
rocy
clina
stell
ata
stella
risA.
stell
ata
buek
kens
isA.
stell
a ste
llaNu
mm
ulite
s hor
moe
nsis
N. st
riatu
sN.
lyell
iN.
bied
aiNu
mm
ulite
s sp.
Assil
ina ex
. gr. a
lpina
Oper
culin
a ex
. gr. g
omez
iOp
ercu
lina
sp.
Hete
roste
gina
arm
enica
arm
enica
H. a
rmen
ica tig
risen
sisH.
retic
ulata
tron
ensis
Hete
roste
gina
sp.
Gyro
idine
lla m
agna
Fabia
nia ca
ssis
Aste
riger
ina ro
tula
Spha
erog
ypsin
a glo
bula
Silve
striel
la te
traed
raCh
apm
anina
gas
sinen
sisEo
annu
laria
eoce
nica
Halky
ardia
sp.
Orbit
olite
s sp.
Linde
rina
sp.
Gyps
ina sp
.pla
nkton
ic for
amini
fera
Ortho
phra
gmine
sAl
veoli
nids
Milio
lids
Textu
larids
Bryo
zoan
sCo
rallin
e red
alga
eCo
rals
Gastr
opod
sEc
hinoid
sCr
inoids
Biva
lves
SO
ĞU
CA
K F
OR
MAT
ION
uppe
r Bar
toni
an18
B18
A
Ceyla
n F
m.
SBZ
STAG
EUN
IT
? ?
Figuer 15. Distribution of benthic foraminifera and other fossil
groups in section PIR (Pırnar, Soğucak Formation).
43
E. ÖZCAN ET AL.
9), gradually passing into the Çengelli Formation,was dated as
early Priabonian (SBZ 19A Zone)(Özcan et al. 2007a). Two samples
from thestratigraphically lower parts of the Doluca Hilllimestone
(DOL 1 & 2) contain mainly small
Nummulites, orthophragmines and coralline redalgae, suggesting
an inner to middle shelfdepositional environment, unlike the
uppermostpart of the sequence, which is dominated by
fore-reeftalus. The foraminiferal assemblage of the Soğucak
-
17
14
23
40
33
11
8
7
İbrice Limanı
Saros Bay13
Mecid
iye
B. Derin Dere
K. Derin Dere24
1
234-5
6-12
1413
15-23
28-32
25-27
34
35
3637
38-39
40-40A
N 1 km
2 31
4 5
33
41
Figure 16. The geological map of Mecidiye region and location of
samples. 1− metamorfics, 2− Fıçıtepe Formation, 3−Soğucak
Formation, 4− Miocene units, 5− aluvium.
44
EOCENE FORAMINIFERA OF THE THRACE BASIN
Formation at Doluca Hill and its close vicinity iscomposed of
taxa listed in Figure 18. These samplesare assigned to the SBZ 18
or19A Zones (lateBartonian or early Priabonian), based both on
theoccurrence of Heterostegina and the early Priabonianage data
from the upper part of the same sequence(Özcan et al. 2007a).
Çengelli FormationThe Çengelli Formation can be traced across
thesouthern part of the Thrace Basin from south ofYeniköy in the
west to Mürefte in the east (Figures 2& 3). This unit is not
known further west thanYeniköy, where the Paleogene shallow to
deepmarine carbonates and clastics are prominent partsof the
Paleogene sequence. A short description of thestudied blocks
(olistoliths), turbidite and marl beds isgiven below.
Olistoliths. The most common blocks in the ÇengelliFormation,
found in virtually all outcrop areas, areBartonian−Priabonian.
Unlike the mixed clastic-carbonate lithologies of the Dişbudak
series, they arecomposed of white thickly bedded to
massivelimestone. The sections and samples characterizingthese
olistoliths are MÜF.C, YEN, 2B, 616, 638 and1902 (Figures 2 &
3).
Section MÜF (Mürefte) C. A 30-metres-thick sectionwas measured
in a large block exposed north of DeveHill (Figure 3) consisting of
monotonous coral andcoralline red algal limestone (MÜF.C,
UTMcoordinates: 0517497, 4505958). Isolated specimensof larger
foraminifera can only be obtained from asingle level (sample MÜF C
6). The only age-diagnostic group is represented by
reticulateNummulites, belonging to N. hormoensis, although
-
MECİDİYE (MEC)
SAMPLES
Orbit
oclyp
eus v
arian
s sca
laris
Aste
rocy
clina
stell
ata i
ndet.
ssp.
Num
muli
tes f
abian
iiNu
mm
ulite
ssp.
Hete
roste
gina
grac
ilisH.
retic
ulata
cf. m
ossa
nens
isH.
retic
ulata
Spiro
clype
us ca
rpat
icus
Spiro
clyeu
ssp.
Gyro
idine
lla m
agna
Fabia
nia ca
ssis
Aste
riger
ina ro
tula
Spha
erog
ypsin
a glo
bula
Silve
striel
la te
traed
raCh
apm
anina
gas
sinen
sisEo
annu
laria
eoce
nica
Halky
ardia
sp.
Gyps
inasp
.Pl
anor
bulin
a sp
.Or
thoph
ragm
ines
Milio
lids
Textu
larids
Bryo
zoan
sCo
rallin
e red
alga
eCo
rals
Gastr
opod
sEc
hinoid
sCr
inoids
Biva
lves
SO
ĞU
CA
K F
OR
MAT
ION
uppe
r Pria
boni
an20
4140A40393837363534333231302928272625242322212019181716151413121110987654321
SBZ
STAG
EUN
IT
Figure 17. Distribution of benthic foraminifera and other
fossilgroups in samples from Mecidiye region (samplesMEC, Soğucak
Formation).
Figure 18. Distribution of benthic foraminifera and other
fossilgroups in samples DOL 1 and 2 in the lower, and insamples ŞAR
2, 4, 9 (data from Özcan et al. 2007a) inthe upper part of the
Soğucak Formation nearDoluca Hill (Şarköy).
Discocyclina augustae olianaeD. aff. augustaeD. trabayensis cf.
elazigensisD. t. ex. interc. elazigensis-trabayensisD. dispansa
umblicataD. pratti cf. prattiD. pratti ex. interc. pratti-minorD.
radians indet. ssp.D. nandoriNemkovella daguiniO. varians ex.
interc. scalaris-variansO. varians cf. variansO.
zitteliAsterocyclina stella indet. ssp.A. stella cf. stellaA.
stellata stellarisA. stellata cf. stellarisA. alticostata cf.
alticostataA ferrandeziNummulites incrassatusNummulites
sp.Heterostegina r. mossanensisHeterostegina sp.Spiroclypeus
sirottiiOperculina ex. gr. gomeziAssilina ex. gr.
alpinaSphaerogypsina globulaGyroidinella magnaPellatispira
madarasziAsterigerina rotulaGypsina
sp.OrthophragminesTextularidsBryozoansCoralline red algaeCorals
DOL 2
DOL 1
ŞAR.9ŞAR.4 SAMPLE
ŞAR.2
SOĞUCAK FM. low. Pri.
19A18 or 19A
upp. Bar. or low. Pri.
SBZ
STAGE
UNIT SAMPLES FROMDOLUCA TEPE &
ITS CLOSE VICINITY
45
E. ÖZCAN ET AL.
very close to N. fabianii. The foraminiferalassemblage in the
lower part is more diverse andincludes taxa listed in Figure 19
(see also for otherforaminifera in sample MÜF C 6). Based on
thepresence of highly advanced N. hormoensis andHeterostegina sp.,
the foraminiferal assemblages canbe assigned to the uppermost part
of the SBZ 18 (lateBartonian) Zone, although a transitional
positionbetween SBZ 18 and 19 (early Priabonian) Zonescannot be
excluded either.
Samples from Other Olistolits. A set of samples werecollected
from olistolith outcrops south of Yeniköy(Figure 2), represented
mainly by foraminiferal(small-sized Nummulites, miliolids
andorthophragmines) and coralline algal limestones.The list of
foraminifera and other fossil groups fromthese olistoliths is shown
in Figure 20. These groupsindicate an inner to outer shelf
depositionalenvironment for these blocks.
-
�6 5
3 2
4Or
bitoc
lypeu
s var
ians i
ndet.
ssp.
Num
muli
tes h
orm
oens
isNu
mm
ulite
ssp.
Assil
inaex
. gr. a
lpina
Hete
roste
gina
sp.
Gyro
idine
lla m
agna
Silve
striel
la te
traed
raCh
apm
anina
gas
sinen
sisFa
biania
cass
isPe
llatis
pira
mad
aras
ziEo
annu
laria
eoce
nica
Glom
alveo
lina
unga
roi
Aste
riger
ina ro
tula
Spha
erog
ypsin
a glo
bula
Halky
ardia
sp.
Gyps
inasp
.
Ortho
phra
gmine
sMi
liolid
sTe
xtular
idsBr
yozo
ans
Cora
lline r
ed al
gae
Cora
lsEc
hinoid
sCr
inoids
Biva
lves
SBZ
18
sample
SBZ
SECTION MÜF.C
1
STAG
E
up
per
BAR
TONI
AN
?
ÇEN
GELL
İOL
ISTO
LITH
UNIT
Figure 19. Distribution of benthic foraminifera and other fossil
groups in section MÜF (Mürefte) C (olistolithin Çengelli
Formation).
46
EOCENE FORAMINIFERA OF THE THRACE BASIN
A succession 25-metres-thick (samples YEN 1-4,UTM coordinates:
0500905, 4499155, Figure 1) wasmeasured in Eocene limestones at
Cinbasarkale Hill.These samples yielded foraminiferal taxa (Figure
20)and, based on the occurrence of Nummulites
fabianii,Heterostegina reticulata mossanensis andAsterocyclina
ferrandezi in sample YEN 2, thisolistolith was assigned to the SBZ
19A (earliestPriabonian) Sub-zone.
Another nearby olistolith (UTM coordinates:0500951, 4499494,
Figure 21) is a composite blockwith pink pelagic limestone and
chert overlain by 5metres of Eocene basal conglomerate and
limestone.Three samples from this Eocene limestone (YEN 7-9)
contain orthophragmines and small-sizedNummulites sp. as the
dominant biogeniccontributors. The occurrence of
Spiroclypeusconfidently establishes the age of the Eocenelimestone
as Priabonian (SBZ 19–20 Zones). Theoccurrence of A. kecskemetii
suggests SBZ 19 ratherthan 20.
Sample YEN 10 was taken from anotherlimestone block due south of
the collecting locality ofsamples YEN 1–4. Taxa from this sample
(Figure 20),and the occurrence of Spiroclypeus establish the ageof
this olistolith as Priabonian (SBZ 19–20 Zones).
Sample 1902, collected due east of Doluca Hill(Figure 3) yielded
an association of Discocyclina
pratti, D. dispansa, D. augustae, Orbitoclypeusvarians cf.
scalaris, Heterostegina reticulata reticulata,and Pellatispira
madaraszi (Figure 20). Theoccurrence of H. r. reticulata
confidently establishesthe age of this olistolith as latest
Bartonian (SBZ18C).
Various small olistoliths from the ÇengelliFormation were
sampled (Samples 2B, 616, 638,Figures 2 & 3). Identified taxa
from their faunal andfloral composition (Figure 20) do not yield a
preciseage for these blocks and they can only be referred
toBartonian or Priabonian.
Samples from the Turbidite Beds of the ÇengelliFormation. Some
turbidite beds of the ÇengelliFormation consist of redeposited
tests of largerforaminifera and other fossil groups, and do
notpermit a high-resolution biostratigraphic scheme,since only a
few larger foraminifera identified inthese beds have a
stratigraphic range covering thewhole duration of the Bartonian and
Priabonian.The distribution of fossil groups in ten levels(samples
ŞAR 10, 11, 12, 13, 172, 649, 202, 183 and428) are shown in Figure
20. Sample 428,representing the uppermost part of the
ÇengelliFormation (Okay et al. 2010), contains mostlycoralline red
algae, bryozoans and corals and it is
-
very probable that this level is Priabonian, in view ofthe early
Priabonian age data from stratigraphicallylower levels (Özcan et
al. 2007a). Foraminifera in theother samples are not age-diagnostic
either, but theoccurrence of Operculina ex. gr. gomezi,Chapmanina
gassinensis, Heterostegina andGyroidinella magna implies a
Bartonian orPriabonian age. Some of the turbidite beds of theunit
contain reworked late Cretaceous pelagic fauna(mainly
Globotruncanidae). Okay & Tansel (1992)presented similar
evidence from blocks in theÇengelli Formation.
Samples from the Marls of the Çengelli Formation.Seven samples
collected from the marls of theÇengelli sequence to investigate
their nannoflora andplanktic foraminifera (listed in Figure 22)
include
Disc
ocyc
lina
augu
stae
D. p
ratti
D. d
ispan
saOr
bitoc
lypeu
s var
ians s
calar
isO.
varia
ns cf
.sca
laris
O. va
rians
O. zi
tteli
Aste
rocy
clina
keck
emet
iiAs
tero
cycli
naaff
.pria
bone
nsis
Afe
rrand
ezi
Num
muli
tes f
abian
iiNu
mm
ulite
ssp.
Hete
roste
gina
r. mos
sane
nsis
H. r.
retic
ulata
Hete
roste
gina
sp.
Spiro
clype
us sp
.Op
ercu
lina
ex. g
r. gom
ezi
Spha
erog
ypsin
a glo
bula
Gyro
idine
lla m
agna
Silve
striel
la te
traed
raCh
apm
anina
gas
sinen
sisFa
biania
cass
isPe
llatis
pira
mad
aras
ziEo
annu
laria
eoce
nica
Glom
alveo
lina
unga
roi
Aste
riger
ina ro
tula
Plan
orbu
lina
sp.
Orbit
olite
ssp.
Pene
ropli
ssp.
Gyps
inasp
.Ro
talia
sp.
Halky
ardia
sp.
Ortho
phra
gmine
sMi
liolid
sTe
xtular
idsBr
yozo
ans
Cora
lline r
ed al
gae
Dasy
clada
cean
alga
eCo
rals
Gastr
opod
sEc
hinoid
sCr
inoids
Biva
lves
YEN.4YEN.3YEN.2
SAMPLE
YEN.1
YEN.10
SAR.13
YEN.9
SAR.12
SAR.10SAR.11
YEN.8YEN.7
202649
sam
ples f
rom
the
turb
iditic
leve
ls of
Çen
gelli
F
orm
ation
sam
ples f
rom
the
limes
tone
blo
cks o
f Çen
gelli
Form
ation
2B
172
183
616638
?
?
SAMPLES FROM OLISTOLITHS & TURBIDITE LEVELS OF ÇENGELLİ
FM.
PRIA
BONI
AN
STAGE
BART
ONIA
N or
PRI
ABON
IAN
428
1902 upp.
BAR.
Figure 20. Distribution of benthic foraminifera and other fossil
groups in samples from the olistoliths and turbidite levelsof the
Çengelli Formation.
YEN 7
YEN 9YEN 8
CB
A
Figure 21. Overview of a composite olistolith in the
ÇengelliFormation south of Yeniköy. Samples YEN 7-9represent the
lower part of the platform limestone(C) above a basal conglomerate
(B). Theseunconformably overlie the red pelagic limestonesequence
(A).
47
E. ÖZCAN ET AL.
-
Helicosphaera euphratis HaqH. compacta Bramlette &
WilcoxonH. intermedia MartiniH. seminulum Bramlette &
SullivanDiscolithina multipora (Kamptner)Transversopontis pulcher
(Defl.)Isthmolithus recurvus Defl.Cyclicargolithus floridanus (Roth
& Hay)Reticulofenestra placomorpha (Kamptner)R. callida
(Perch-Nielsen)R. bisecta (Hay et al.)R. placomorpha
(Kamptner)Chiasmolithus grandis (Bramlette & Riedel)C. cf.
grandis (Bramlette & Riedel)Chiasmolithus sp. (older
type)Coccolithus pelagicus (Wallich)C. eopelagicus (Bramlette &
Riedel)Cyclococcolithus formosus KamptnerZygrhablithus bijugatus
(Defl.)Lanternithus minutus StradnerBraarudosphaera bigelowi (Gran
& Braarud)Micrantholithus vesper Defl.Discoaster tani Bramlette
& RiedelD. cf. tani Bramlette & RiedelD. cf. binodosus
MartiniD. lodoensis Bramlette & RiedelD. distinctus MartiniD.
cf. distinctus MartiniD. cf. mirus Defl.D. barbadiensis TanD.
deflandrei Bramlette & RiedelSphenolithus radians Defl.S.
predistentus Bramlette & WilcoxonS. moriformis (Brönn. &
Stradner)S. radians Defl.Blackites sp.
REWORKED NANNOFOSSILS
Eiffellithus turriseiffeli (Defl.)Eiffellithus eximius
(Stover)Watznaueria barnesae (Black)Arkhangelskiella sp.
Globorotalia bullbrooki (Bolli)G. cerroazulensis frontosa
(Subbotina)G. cerroazulensis cerroazulensis (Cole)G. cerroazulensis
pomeroli Toumarkine et BolliG. cf. c. possagnoensis Toumarkine et
BolliGlobigerina cryptomphala GlaessnerG. eocaena GümbelG.
corpulenta SubbotinaG. hagni GohrbandtG. linaperta Finlay
Globigerina sp.Globigerinatheka index index (Finlay)G. cf.
luterbacheri BolliGlobigerinita martini martini Blow et
BannerTruncorotaloides cf. rohni Broennimann et Bermudez
1907
1901 SAMPLE
1900
ÇENGELLİ FM. upper Eo.-lower Rup.
19-2216-22
Bartonian-lower Rupelian
NP
STAGE
UNIT SAMPLES FROMMARLS OF ÇENGELLİ
FORMATION
PLANKTONIC FORAMINIFERA
CALCAREOUS NANNOPLANKTON
ÇEN.2
16-21 ŞAR.4
ŞAR.17
ŞAR.2007 -B
Figure 22. Distribution of calcareous nannoplankton and
planktonic foraminifera in the marlybeds of the Çengelli
Formation.
48
EOCENE FORAMINIFERA OF THE THRACE BASIN
-
49
E. ÖZCAN ET AL.
four from near Doluca Hill, where the Çengelli seriesclearly
overlies the Soğucak Limestone. These are(Figure 3) samples 1900,
1901 and 1907 from north-east of Doluca Hill and ÇEN.2 from west of
the hill.The calcareous nannoflora from sample 1900generally
indicates the Bartonian NP 16-17 Zones,but the older (lower to
middle Eocene) forms such asChiasmolithus cf. grandis, Discoaster
cf. tani and D.cf. binodosus are poorly preserved. Without
theseforms, most other species belong to the NP 16 to NP22 Zones,
i.e. from Bartonian to lower Rupelian. Theassemblage of sample 1901
represents three differentages: (i) Turonian to Campanian, based on
theshortest range of Eiffellithus eximius, (ii) late Ypresianto
earliest Lutetian (NP 12-14), indicated by theshortest range of
Discoaster lodoensis, (iii)Priabonian to earliest Oligocene (NP
19-22)determined by the range of Isthmolithus recurvus.The other
marker species for the end of NP 20 or NP21 (Discoaster
barbadiensis, Cyclococcolithusformosus) may be reworked from older
Eocene beds.The above assemblages of three different ages alsooccur
in sample 1907. Its age (NP 19-22, Priabonianto earliest Oligocene)
is defined by the range ofIsthmolithus recurvus. There are reworked
olderforms from the Cretaceous (Turonian to Campanianwith
Eiffellithus eximius) and from the older (lowerto middle ?) Eocene
with Sphenolithus radians,Helicosphaera seminulum and Discoaster
div. sp. Inthe poor nannoplankton assemblage of sampleÇEN.2
Reticulofenestra placomorpha has the shortestrange: NP 16 – NP 22,
i.e. Bartonian to lowerOligocene. The age of the rather poor
plankticforaminifera from samples 1900 and 1901 is middleEocene,
while those of samples 1907 and ÇEN.2,containing much richer
assemblages, span fromBartonian to early Priabonian (P 14-15). To
sum up:The Çengelli Formation near Doluca Hill consists ofmixed
planktonic assemblages, among which theyoungest forms approach most
reliably the real age ofthese olistostromal deposits. Therefore,
the age of theÇengelli Formation is considered to be
middlePriabonian to earliest Rupelian (NP 19-22). This fitswith the
youngest age (early Priabonian, Özcan et al.2007a) from the
underlying Soğucak Limestone.
The other three samples (ŞAR.4, UTM: 0501126,4499536; ŞAR.17,
UTM: 0500825, 4498777 andŞAR.2007B from the matrix of the
olistostrome ofsamples YEN 7-9 with the same UTM co-ordinates,see
above) are from near Yeniköy (Figure 2). Theyyielded poorer
nannoflora, giving an age fromBartonian to earliest Rupelian (NP
16-21), whereasplanktonic foraminifera are rare and recrystallized
oraltogether absent (as in sample ŞAR.17) and give avery uncertain
middle Eocene age. Since thepresence of Spiroclypeus (first
appearing in the upperEocene) in the olistoliths clearly indicates
that thematrix cannot be older than Priabonian as well, mostof the
plankton from the matrix has to be consideredas redeposited in this
case, too. The upper age of theolistostrome in the Yeniköy region
is given byCylococcolithus formosus, last occurring in the NP
21Zone, approximately marking the Eocene/Oligoceneboundary.
Keşan FormationLarger foraminifera occur very sporadically in
thedeep marine Keşan (Ceylan) Formation. In southernThrace, a
rather rich assemblage has been discoveredonly in one locality near
Çeltik village (Figure 1B).This sandstone sample (ÇEL 13, UTM
coordinates:06366, 03036) contains Heterostegina reticulataitalica,
the most advanced stage of the species in thePriabonian, Nummulites
budensis, Operculina ex. gr.gomezi and Linderina sp. This
assemblage suggests amiddle to late Priabonian (SBZ 19B-20) age for
thissample.
Systematic PaleontologyIn this section, systematic description
ofstratigraphically important groups such asorthophragmines and
nummulitids (e.g.Heterostegina, Spiroclypeus and some Nummulites)
isgiven. Some comments on the occurrence of otheraccompanying
benthic foraminifera identified in theÇengelli and Soğucak
formations are made in thesection ‘Conclusions’. Some taxa such as
Discocyclinadiscus, D. trabayensis, Nemkovella evae and N.
-
strophiolata, are represented by one single specimenin our
material and are therefore not described here.The description of
the two Discocyclina species,more widely recorded from the northern
part of theThrace Basin, can be found in Less et al. (in
review),whereas that of the Nemkovellae is in Özcan et
al.(2007b).
Since most of the taxa occurring in our materialwere described
in detail in the last few years, we donot repeat their description
here. The mostcomprehensive data for Western TethyanHeterostegina
and Spiroclypeus, with their newlyproposed taxonomic and
phylogenetic scheme, aregiven in Less et al. (2008) and Less &
Özcan (2008).A synthesis of diagnostic features of
Tethyanorthophragminid families and genera and theirqualitative
features can be found in Less (1987,1993), Less et al. (2007), Less
& Ó. Kovács (2009) andÖzcan et al. (2007a, b). Additional
information withreferences to more detailed descriptions,
geographicand stratigraphic ranges, and the most
up-to-datesubdivision into subspecies in orthophragmines canbe
found in Less (1987, 1998a), Less et al. (2007),Less & Ó.
Kovács (2009), Özcan (2002), Çolakoğlu &Özcan (2003) and Özcan
et al. (2007a, b). The mostup-to-date description of most
orthopragminidspecies discussed below can be found in Özcan et
al.(2007a); for Discocyclina archiaci, D. fortisi,Orbitoclypeus
schopeni and O. munieri see Özcan etal. (2007b) while for D.
seunesi, Nemkovella stockariand O. bayani see Less et al. (2007). A
shorteneddescription is given for Orbitoclypeus haynesi
andAsterocyclina aff. priabonensis, fully described bySamanta &
Lahiri (1985) and Less (1987),respectively. A complete description
is given only forO. zitteli, since this taxon is hardly mentioned
sinceChecchia-Rispoli (1909). A revised stratigraphy oflate
Paleocene to Priabonian orthophragmines isproposed in Less et al.
(2007) and Özcan et al.(2007a, b). An updated range-chart for the
above andother stratigraphically important benthic taxa thatcover
the late Lutetian to early Rupelian interval isshown in Figure 23.
Based on Less et al. (2008) thesubdivision of reticulate Nummulites
(N. fabianiilineage), spanning from the early Bartonian to
themiddle Oligocene, is shown in Figure 24.
Principles in the Determination ofOrthophragmines and
NummulitidsIn the description of orthophragmines we adoptedthe
principles used by Less (1987, 1993) as illustratedin Figure 25A,
and explained in the header of Tables1−3. A synopsis of subspecies
identification based onthe outer cross-diameter of the
deuteroconch(parameter d) is shown in Figure 26. Thedetermination
of Nummulites is based on both thesurface characteristics and the
features of the
Oligocene
earlyLutetian Rupelian
A B C A B?
N. brongniarti-puschi-groupN. gizehensis-lyelli-groupN.
millecaput-maximus-groupN. perforatus-biedai-groupN.
lorioli-ptukhiani-groupN. bullatusN. garganicusN. hormoensisN.
fabianiiN. fichteliN. discorbinus-beaumonti-groupN. striatus ?N.
incrassatusN. chavannesiN. pulchellusN. stellatus ?N. vascus
?A. spira-groupA. exponens-groupA. schwageri ?A. alpina ?O.
gomezi-groupO. complanata ?H. armenica armenicaH. armenica
tigrisensisH. reticulata tronensisH. reticulata hungaricaH.
reticulata multifidaH. reticulata helveticaH. reticulata
reticulataH. reticulata mossanensisH. reticulata italica ?H.
gracilisS. sirottiiS. carpaticus
?
Other orthophragmines (D. dispansa, D. augustae, D. radians, D.
trabayensis, O.
varians, O. furcatus, A. stella, A. stellata)
20 21
Orthophragmines of Lutetian acme (D. pulcra, Orbitoclypeus
douvillei)
Discocyclina discus
Orthophragmines of middle Eocene acme (D. pratti, Nemkovella
strophiolata, Asterocyclina
alticostata, A. kecskemetii)Orthophragmines of Priabonian acme
(D. euaensis, D. nandori, D. aspera, D. ruppi,
A. ferrandezi, A. priabonensis)
Oper-culina
H e
t e
r o s
t e g
i n
aR
etic
ulat
e N
umm
ulite
s
Shallow benthic zones (SBZ) 16 17
Spiro-clypeus
Pellatispira
Rad
iate
Num
mul
ites
Nummulites garnieri-groupGiant
AssilinaSmall
Assilina
E o c e n e
19
Alveolina
Gia
nt
Num
mul
ites
18
m i d d l e l a t ePriabonian B a r t o n i a n
Figure 23. Range-chart for some late Lutetian to early
Rupelianlarger benthic foraminiferal taxa of the WesternTethys. The
subdivision of the stratigraphic scale isnot time-proportional
(Less et al. 2008).
50
EOCENE FORAMINIFERA OF THE THRACE BASIN
-
Taxon Pmean ( m) Surface Stage SBZ zoneN. bullatus 65–100
granules, no reticulation basal Bartonian early SBZ 17
N. garganicus 100–140 heavy granules + reticulation early
Bartonian to middle late Bartonianlate SBZ 17 to SBZ 18B
N. hormoensis 140–200 heavy granules + umbo + reticulation late
Bartonian SBZ 18N. fabianii 200–300 heavy reticulation, weak
granules + umbo Priabonian to early Rupelian SBZ 19–21N. fichteli
200–300 weak reticulation to irregular mesh late Priabonian to late
Rupelian SBZ 20–22AN. bormidiensis 300–450 irregular mesh early
Chattian SBZ 22B
Figure 24. Subdivision of the Nummulites fabianii-lineage in the
Bartonian to early Chattian time-span (Özcanet al. 2009). SBZ
21–22B are in the sense of Cahuzac & Poignant (1997).
P
D
Md
dM
D
+++
++
++
+
+
+
+++
++ + +
++*
* * * **
**
*
***
*d
P
BApd
H
W
n
w
h
C
Figure 25. Measurement system for megalospheric larger
foraminifera (parameters are explained in the headers of Tables 1to
5). The parameters for the definition of megalospheric
orthophragmines (A), Nummulites (B), Heterosteginaand Spiroclypeus
(C).
51
E. ÖZCAN ET AL.
equatorial section. Based on Drooger et al. (1971),Less (1999)
introduced a measurement andparameter system to characterize the
equatorialsection of A-forms that is slightly modified here(Figure
25B). These parameters adopted here areexplained in the header of
Table 4 (also see Figure25). The description of Heterostegina
andSpiroclypeus is based on the system introduced byDrooger &
Roelofsen (1982) and adopted for Eocenerepresentatives of these
genera (Less et al. 2008 andLess & Özcan 2008). The explanation
ofmeasurements and counts executed in the equatorialsection of each
megalospheric specimens (Figure25C) are given in the header of
Table 5.
Biometric data are summarized in Tables 1−5.Grouped samples
containing almost the sameassemblages having similar parameters are
evaluated
both separately and jointly. However, the
subspecificdetermination of particular species is given for
thejoint samples on the basis of the total number ofspecimens.
These data are marked always with boldletters. Because of limited
space, a completestatistical evaluation with the number of
specimens(n°), arithmetical mean and standard error (s.e.) isgiven
only for deuteroconch size (d), the crucialparameter in subspecific
determination. Subspeciesare determined according to the
biometrical limits ofsubspecies for populations presented in
thedescription of the given species. No subspecies isdetermined if
only a single specimen is availablefrom joint samples. If the
number of specimens istwo or three, the subspecies is determined as
cf. Ifthis number is four or more, however the dmean valueof the
given population is closer to the biometrical
-
Equatorial chamberlets
number width height annuli/0.5 mm width height
N W ( m) H ( m) n w ( m) h ( m)Species Sample mean range range
range range range range
Discocyclina seunesi SAZ 46 6 225 – 450 341.7 ± 34.9 140 – 270
203.3 karabuekensisMÜF A 10 10 280 – 470 380.0 ± 19.2 150 – 240
197.5 17–30 35–40 45–70 11–13 35–45 80–85
staroseliensis–archiaci1894 9 380 – 650 503.3 ± 29.1 170 – 320
232.9 28–38 30–50 40–60 11–12 25–35 45–65 archiaci
D. discus GIZ A 4 1 1030.0 430.0 indet. ssp.MÜF A 10 28 530 –
1040 726.3 ± 23.7 250 – 630 379.4 51–63 30–50 55–80 6–9 35–45
65–100 fortisi1894 21 540 – 1005 723.8 ± 20.8 290 – 520 376.7 53–61
30–50 40–85 7–9 30–50 50–75 fortisiMÜF A 10 8 90 – 115 106.3 ± 2.8
55 – 85 66.3 10–11 15–35 15–25 16–21 20–25 70–85 sourbetensis1894 4
90 – 125 107.5 ± 6.7 65 – 85 76.7 10 15–20 15–20 16–20 25–30 50–55
sourbetensisGIZ A 9+11 16 130 – 215 163.1 ± 5.8 70 – 110 95.4 20 35
30 50 13 18 20 35 50 95
GIZ A 9 9 130 – 215 160.0 ± 8.3 70 – 100 92.9 20 35 30 50 13 18
20 35 50 90GIZ A 11 7 130 – 190 167.1 ± 7.7 80 – 110 98.3 30 35 35
40 15 25 30 95
GIZ A 12 7 140 – 190 160.7 ± 5.8 85 – 115 100.0 25 40 35 60 15
25 35 50 55 atlanticaPIR 46 4 195 – 240 221.3 ± 9.7 100 – 125 110.0
olianae-augustaePIR 47A+48 14 190 – 225 206.1 ± 2.9 100 – 130
116.3
PIR 47A 3 205 – 225 213.3 110 – 130 120.0PIR 48 11 190 – 225
204.1 ± 3.1 100 – 125 115.0
1902 1 210.0 100.0 indet. ssp.1894 4 170 – 250 216.3 ± 14.7 90 –
125 106.3 16–20 30–35 35–45 13–16 20–25 50–70 tauricaGIZ A 6+7 4
315 – 345 331.3 ± 6.0 150 – 160 155.0 35 55
GIZ A 6 1 345.0 160.0 55GIZ A 7 3 315 – 340 326.7 ±
