Turkish Journal of Earth Sciences
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Research Article

Turkish J Earth Sci
(2013) 22: 143-171
© TÜBİTAK
doi:10.3906/yer-1107-2

Late Maastrichtian-Late Palaeocene planktic foraminiferal biostratigraphy of the matrix
of the Bornova Flysch Zone around Bornova (İzmir, Western Anatolia, Turkey)
Bilal SARI*
Dokuz Eylül University, Faculty of Engineering, Department of Geological Engineering, Tınaztepe Campus, 35160, Buca-İzmir, Turkey
Received: 17.07.2011

Accepted: 15.02.2012

Published Online: 04.01.2013

Printed: 25.01.2013

Abstract: The Bornova Flysch Zone (BFZ), located between the Menderes Massif and the İzmir-Ankara Suture in westernmost Anatolia
(Turkey), forms the westernmost part of the Anatolide-Taurides. The BFZ comprises intensely sheared Upper Cretaceous-Palaeocene
matrix and blocks of various origins. The matrix of the BFZ is mainly made up of unfossiliferous flysch-type sediments (alternations of
sandstones and shales). In Bornova (İzmir, western Turkey) and its surroundings, these clastics locally include planktic foraminiferabearing pelagic micritic limestone and calcareous shale lenses and interbeds (Beytitepe Limestone). As a result of studies focusing on the
planktic foraminifera-bearing pelagic interlayers in three areas (Gökdere, Işıklar and Kocaçay areas) around Bornova, a detailed planktic
foraminiferal biostratigraphy of the rocks is documented for the first time. The thickness of the laminated micritic limestones attains
360 m in the Gökdere area. Occurrences of late Maastrichtian species such as Abathomphalus mayaroensis (Bolli), Contusotruncana
contusa (Cushman), Globotruncanita conica (White) and Racemiguembelina fructicosa (Egger) within planktic foraminifera assemblages
obtained from the laminated micritic limestones and red calcareous shales in the three areas suggest a late Maastrichtian age for these
rocks. The occurrence of various species of Globanomalina, Morozovella, Igorina and Parasubbotina within the calcareous shales in

the Işıklar area suggests a late Palaeocene age. The Kocaçay area has well-preserved outcrops showing the stratigraphy of the matrix,
despite the more complex geology. The upper Maastrichtian laminated micritic limestones are gradationally overlain by upper
Maastrichtian calcareous shales. The calcareous shales are represented by rich planktic foraminiferal assemblages and include blocks
derived from laminated micritic limestones. The upper Mastrichtian calcareous shales are overlain by Palaeocene red calcareous shales.
Poor assemblages including Parasubbotina varianta (Subbotina), Subbotina triangularis (White), Subbotina cf. velascoensis (Cushman),
Globanomalina compressa (Plummer) and Globanomalina planoconica (Subbotina) indicate a late Palaeocene age for the lower part and
a latest Palaeocene age for the upper part of the calcareous shale sequence. Therefore, the age of conglomerates and flysch overlying the
calcareous shales should be latest Palaeocene or younger in the Kocaçay area.
Key Words: Planktic foraminifer; biostratigraphy; late Maastrichtian - late Palaeocene; Bornova Flysch Zone; Western Anatolia

1. Introduction
The Bornova Flysch Zone (BFZ) forms a 50 to 90 km wide
and approximately 230 km long tectonic zone between
the Menderes Massif and the İzmir-Ankara Suture (Okay
& Altıner 2007) in westernmost Turkey (Figure 1). It
corresponds to the western part of the İzmir-Ankara Zone
of Brinkmann (1966). The rocks of this zone cropping out
in İzmir and its surroundings were named the Bornova
mélange by Erdoğan (1990b). According to Okay et al.
(2012) the Upper Cretaceous rocks of the BFZ were
deposited in a narrow basin on the northern margin of
the Anatolide-Tauride Block located between the NeoTethyan Ocean to the west and a strike-slip tear fault to
the east. As the tear fault separated the basin fill and the
continental subduction zone to the east, the BFZ escaped
Tertiary metamorphism while the coeval rocks of the
Menderes Massif underwent HP/LT metamorphism.
*Correspondence:

The BFZ comprises intensely sheared matrix and
blocks of Mesozoic limestone, mafic volcanic rocks,

radiolarites and serpentinites (Erdoğan 1990b; Okay &
Siyako 1993). The limestone blocks derived from the
platform range up to 20 km across and their ages range
from Triassic to Late Cretaceous (Özer & İrtem 1982;
Özer 1989; Erdoğan 1990a, 1990b; Erdoğan et al. 1990;
Okay & Siyako 1993; İşintek et al. 2000; İşintek et al. 2006;
Okay & Altıner 2007; Senowbari-Daryan & İşintek 2008;
İşintek et al. 2009a, 2009b). The matrix of the BFZ in the
İzmir area comprises mainly unfossiliferous flysch-type
sediments (alternations of sanstones and shales), which
locally include calcareous shales and micritic limestone
lenses and interbeds with planktic foraminifera suggesting
a Campanian-early Palaeocene (Danian) age according
to previous studies (Konuk 1977; Yağmurlu 1980; Özer &
İrtem 1982; Erdoğan 1990b).

143


Sarı-Figure 1
SARI / Turkish J Earth Sci

a

Rhodope-Stranja
Massif

42°

Black Sea

Thrace
Basin

e

Zon

İstanbul

ul

İstanb
Sea of Marmara

lag

Pe

Sakarya

Zone

on

Tavşanlı Zone

ian

IAS


Zo

Afyon Zone
BF
Z

ne

Aegean
Sea
38°

Menderes
Massif

İzmir

Figure 1b

Athens

Lycian
Nappes

N
Cycladic
Islands
BFZ: BORNOVA FLYSCH ZONE
IAS: İZMİR-ANKARA SUTURE


b

10000

20000

Yamanlar
Dağı

Q
Balatçık
Çiğli

60000

200 km

Mediterranean Sea

Spil
Dağı

Kocaçay
area

Bornova

Karşıyaka

İzmir


İzmir Bay

N

30000

Işıklar
area

Kemalpaşa

Q

Narlıdere

50000

Buca

Balçova
Güzelbahçe

Gökdere
area
Mahmut
Dağı

Dağkızılca
40000


Q

Efemçukuru

10 km

Cumaovası

Q
alluvium

Neogene Neogene
sedimentary volcanic
rocks
rocks

Cretaceous flysch
and carbonate rocks

Paleozoic-Mesozoic
metamorphic rocks

study
areas

Figure 1. (a) Main tectonic units of western Anatolia and eastern Greece (after Görür & Tüysüz 2001). Study area is situated in the
Bornova Flysch Zone, which corresponds to the westernmost part of the Tauride-Anatolides. (b) Simplified geological map of İzmir
and surroundings, showing locations of the study areas (simplified after Erentöz 1964).


144


SARI / Turkish J Earth Sci

Well-preserved outcrops of calcareous shales and
micritic limestones occur around Bornova (İzmir) and
its surrounding area (Figure 1). These calcareous pelagic
interlayers, named the Beytitepe Limestone by Yağmurlu
(1980), are an unique palaeontological data resource
within the matrix of the BFZ as they yielded rich planktic
foraminifera assemblages. Hence, they possess important
data relating to the opening and closing ages and the
sedimentological and tectonostratigraphic evolution
of the basin. However, few studies have dealt with the
palaeontological aspects of these rocks (Konuk 1977;
Yağmurlu 1980; Özer & İrtem 1982; Erdoğan 1990b). The
planktic foraminiferal content of the pelagic interlayers
has not been documented in detail until today despite its
importance in dating the matrix of the BFZ.
A planktic foraminifera based biostratigraphic study
of the calcareous shales and micritic limestones of the
Beytitepe Limestone is documented here in order to help
chronostratigraphic determinations (Figure 2).
2. Material and methods
This study is based on detailed geological mapping and
systematic sampling through the measured stratigraphic
sections. Four hundred seventy nine samples were
collected from the pelagic micritic limestones and
calcareous shales of the Beytitepe Limestone in order

to study the planktic foraminiferal content. A standard
washed-sample method did not work as the limestones
AGE

Upper Cretaceous
(middle-upper
Santonian)

uppermost Palaeoceneupper Maastrichtian
upper
Maastrichtian

and calcareous shales are mostly indurated and cut by
numerous pressure solution seams as a result of intense
shearing. Therefore, thin sections were prepared from 390
samples, from which axially oriented forms were picked
to identify most taxa with a high degree of confidence, as
most of the diagnostic criteria can be recognized in such
axial and/or subaxial sections. This method is widely
used in planktic foraminifera studies, especially in the
Cretaceous (Wonders 1979; Fleury 1980; Sliter 1989;
Premoli Silva & Sliter 1994; Sliter 1999; Robaszynski et
al. 2000; Premoli Silva & Verga 2004). Papers specific
to Turkey include Farinacci & Yeniay (1986), Özkan &
Köylüoğlu (1988), Özkan Altıner & Özcan (1999), Sarı
(1999), Sarı & Özer (2002), Sarı (2006a, 2006b, 2009)
and Okay & Altıner (2007), which are based on planktic
foraminifera identified in thin section. Hovewer, there
have been few attempts to study Palaeocene planktic
foraminifera from thin section. The resolution of thinsection zonation is nearly as precise as zonal schemes based

on isolated specimens for the Cretaceous (Sliter 1989). In
addition to these contributions, Robaszynski et al. (1984)
is also frequently cited for late Maastrichtian planktic
foraminiferal species identification. The Latest Cretaceous
planktic foraminiferal zonation of Premoli Silva & Sliter
(1994), Premoli Silva & Sliter (1999) and Premoli Silva
& Verga (2004) is followed in this study (Figure 3).
Palaeocene planktic foraminifera identification is based
on Berggren et al. (1995), Olsson et al. (1999) and Olsson

LITHOLOGY LITHOLOGY EXPLANATION

rudist-bearing
bioclastic limestone
planktic foraminifera-bearing
micritic limestone
planktic foraminifera-bearing
calcareous shale
planktic foraminifera-bearing
laminated micritic limestone

conglomerates

UNIT

Işıklar Limestone

Beytitepe
Limestone


STUDIED
INTERVAL

Kocaçay Conglomerate

deformed, highly sheared,
sheared flysch
flysch-type sandstone-mudstone
alternation
(mudstone dominated)
Figure 2. Simplified columnar section of the matrix of the Bornova Flysch Zone around Bornova. This study
focuses on the planktic foraminifera-bearing Beytitepe Limestone, consisting of laminated micritic limestones and
calcareous shales.

145


SARI / Turkish J Earth Sci

146

Thanetian

56

60
61
62
63


PLANKTIC
FORAMINIFERA
BIOZONES
P5 M. velascoensis
P4c Ac. soldadoensisGl. pseudomenardii

P4b Ac. subsphaerica

Selandian

59

EARLY

58

pseudomenardiiP4a Gl.
P. variospira
P3b I. albeari
P3a I. pusilla
P2

P. uncinata

Gl. compressaP1c P. inconstans

Danian

57


PALAEOCENE
LATE

64

P1b S. triloculinoides
P1a P. pseudobulloides

65

Pα & P0 P. eugubina &
G. cretacea

Maastrichtian

66

69
70
71
72
73
74
75
76

C. contusa - R. fructicosa

Ga. gansseri


late

68

A. mayaroensis

early

late

67

Campanian

3. Geological setting and previous studies
The BFZ consists of chaotically deformed CampanianLower Palaeocene flysch-type matrix and blocks of various
sizes and origins (Erdoğan 1990b; Okay & Siyako 1993).
Many of the blocks comprise shallow water limestones,
some of which can be as large as 20 km in diameter.
These limestone blocks were the subject of several studies,
that showed that their ages range from Triassic to Late
Cretaceous (Özer & İrtem 1982; Özer 1989; Erdoğan 1990a,
1990b; Erdoğan et al. 1990; Okay & Siyako 1993; İşintek et
al. 2000; İşintek et al. 2006, 2007; Okay & Altıner 2007;
Senowbari Daryan & İşintek 2008; İşintek et al. 2009a,
2009b). They were stratigraphically and palaeontologically
correlated with the Karaburun Mesozoic successions
(Erdoğan 1990a, 1990b). Some of the neritic blocks
include pelagic interlayers in their stratigraphically upper
parts. A Tithonian-Turonian pelagic level in a block from

south of Bigadiç (NE of the Zone) was documented by
Okay & Altıner (2007), who correlated the stratigraphy of
the block with similar successions from the Lycian nappes
to the south. Turonian-Maastrichtian, CampanianMiddle Maastrichtian and Santonian-Campanian ages
were also recorded from the pelagic parts of the blocks
(Erdoğan 1990b). Blocks of radiolarian cherts also yielded
palaeontological data. Recently, Mid to Late Triassic
(late Ladinian to middle Carnian), Middle Jurassic (late
Bathonian to early Callovian) and Middle Jurassic to Late
Cretaceous (latest Bajocian to late Cenomanian) ages were
documented based on the radiolaria in various chert blocks
by Tekin & Göncüoğlu (2007), Tekin & Göncüoğlu (2009)
and Tekin et al. (2010) respectively. Some palaeontological
studies have data about planktic foraminifera, which give
information on the fossiliferous pelagic interlayers within
the flysch-type rocks of the matrix. A Turonian-Early
Campanian age was documented for the flysch in the
Seferihisar area by Akartuna (1962). A late CampanianMaastrichtian age was obtained from Manisa and its
surroundings by Oğuz (1966). According to Marengwa
(1968), the age of the flysch in the Işıklar area is TuronianCampanian. Konuk (1977) described some planktic
foraminifera assemblages from the Kocaçay area (north
of Bornova, İzmir), where the pelagic calcareous rocks
are late Campanian - late Maastrichtian and are overlain
by Palaeocene or younger conglomerates and flysch
respectively. The calcareous pelagic interlayers were
named the Beytitepe Limestone by Yağmurlu (1980),
who used the stratigraphical positions for three different
flysch formations south of Bornova to establish their
Campanian, Maastrichtian-Early Palaeocene and Middle-


TIME EPOCH AGE
(Ma)

CRETACEOUS
LATE

et al. (2011). Biozonation of Berggren et al. (1995), Olsson
et al. (1999), Berggren & Pearson (2005) and Olsson et al.
(2011) is followed here (Figure 3). Because it is not easy to
separate some Palaeocene species from two dimensional
axial views in thin section, these species are grouped
as Morozovella angulata (White) - Morozovella aequa
(Cushman & Renz) group and Morozovella conicotruncana
(Subbotina) - Morozovella velascoensis (Cushman) group.

G. aegyptiaca
Gl. havanensis
Ra. calcarata

Figure 3. Chronostratigraphic chart showing the latest
Cretaceous-Palaeocene planktic foraminiferal zonation. The
latest Cretaceous zonation plotted against the time scale of
Gradstein et al. (1994) is derived from Premoli Silva & Sliter
(1994), Robaszynski (1998), Premoli Silva & Sliter (1999) and
Premoli Silva & Verga (2004). Palaeocene zonation is from
Berggren et al. (1995), Olsson et al. (1999), Berggren & Pearson
(2005) and Olsson et al. (2011). Time scale is adapted from
Berggren et al. (1995).

Late Palaeocene ages. A Danian age was documented

from nanoplankton assemblages from the Işıklar area by
Özer & İrtem (1982). Erdoğan (1990b) documented a
more detailed planktic foraminiferal data from the matrix


SARI / Turkish J Earth Sci

of the BFZ in the area between Karaburun, Seferihisar
and Manisa. He obtained a Campanian-Maastrichtian
age from the Gökdere area, a Middle MaastrichtianDanian age from the Kocaçay area, an upper Campanianlower Maastrichtian age from the Pınarbaşı section
(SE of Bornova), and a Campanian and middle-late
Maastrichtian age from Spil Mountain (Manisa). İşintek
et al. (2007) examined limestone blocks from the Kocaçay
Conglomerate, which overlies the Palaeocene calcareous
shales in the Kocaçay area. They obtained Late CretaceousPalaeocene, Palaeocene, middle-late Palaeocene ages from
the neritic limestone blocks and suggested that the age of
the conglomerates should be middle-late Palaeocene or
younger.
The base of the pelagic limestones and overlying flyschtype rocks were observed at two localities. The first locality
is from the Karaburun peninsula, where a Mesozoic
(Aptian-Albian) neritic sequence is unconformably
overlain by Lower Campanian to Middle Maastrichtian
pelagic limestones and flysch-type rocks of the Balıklıova
Formation (Brinkmann et al. 1977; Tansel 1990; Erdoğan
1990b; Erdoğan et al. 1990). At the second locality, in the
Kemalpaşa area (east of İzmir), Poisson & Şahinci (1988)
documented the stratigraphy of a Mesozoic block and
suggested that the Mesozoic neritic sequence was overlain
by Maastrichtian pelagic rocks, middle Palaeocene or
younger conglomerates and flysch respectively.

The flysch deposits and the blocks of the BFZ are
unconformably overlain by undeformed upper Lower
Eocene (late Cuisian) neritic limestones north of Akhisar
(Akdeniz 1980; Önoğlu 2000). Therefore deformation
affecting the BFZ must have predated the late Early
Eocene. The rocks of the BFZ are unconformably overlain
by the conglomerates, claystones and clayey limestones of
the Miocene Sabuncubeli Formation in Bornova and its
surroundings (Erdoğan 1990b).
4.
Stratigraphy
and
planktic
foraminiferal
biostratigraphy of the Beytitepe Limestone
The matrix of the BFZ dominantly comprises intensely
sheared flysch-type deposits (alternations of sandstones
and shales), which include conglomerates, micritic
limestones and calcareous shales as lenses or conformable
interbeds (Figure 2). This study focuses on the micritic
limestones and calcareous shales, known as the Beytitepe
Limestone, as they include rich planktic foraminiferal
assemblages (Figure 2). The stratigraphy and planktic
foraminiferal biostratigraphy of the micritic limestones
and calcareous shales of the Beytitepe Limestone were
studied in detail in the Gökdere, Işıklar and Kocaçay areas
around Bornova (Figure 1).
4.1. The Gökdere area
The Gökdere area, covering approximately 12 km2, is
located 10 km southeast of Bornova (Figures 1, 4). The

Beytitepe Limestone occurs as a thick interlayer within
flysch-type rocks and shows significant fluctuations in
thickness over short distances (Figure 4). Numerous levels
of variable thickness and size were also observed within

the flysch. Two stratigraphic sections, the Beytitepe and
the Gökdere sections, were measured from the Gökdere
area. Details of the stratigraphic and palaeontological data
obtained from these measured stratigraphic sections are
presented below.
The Beytitepe stratigraphic section The Beytitepe
Limestone is bounded both below and above by sandstoneshale alternations (Figures 4, 5, 6). The sandstone beds
overlying the limestones show partial Bouma sequences.
The Beytitepe Limestone consists of grey laminated
micritic limestones (Figure 7a). Pinkish grey and pale
greenish-grey interlayers were also observed. Lamina
thickness is millimetric to centimetric. Fifty nine samples
were collected through the section. The carbonate content
of the sandstone-shale alternation increases towards the
flysch-limestone contact and flysch gradually passes into
the laminated limestones at the bottom of the sequence
(Figure 6). Neritic blocks and sand-size clasts were
observed at the base of the micritic limestones. In addition,
reworked orbitoid benthic foraminifera were also observed
throughout this level. The limestones have a planktic
foraminiferal mudstone/wackestone depositional texture
(Figures 7c, d). The abundance of planktic foraminifera
varies from sample to sample (Figure 6). Some levels were
severely affected by intense shearing. As a result, rock and
the planktic foraminifera were cut by pressure solution

seams (Figure 7d). However, some levels escaped the effect
of shearing, and many complete specimens of planktic
foraminifera were observed (Figure 7c). An echinoid
fragment was observed 149 m above the section base
(Figures 6,7b). The specimen belongs to the holasterid
group and probably is a species of the genus Echinocorys
(Andy Gale, Pers. comm. 2010). The laminated micritic
limestones of the Beytitepe stratigraphic section mostly
have a moderate to poor planktic foraminifera content. But,
some rich planktic foraminifera-bearing levels were also
observed (Figure 6). The following planktic foraminifera
were observed in the Beytitepe stratigraphic section:
Abathomphalus mayaroensis (Bolli), Contusotruncana
contusa (Cushman), C. fornicata (Plummer), C.
patelliformis (Gandolfi), Contusotruncana walfischensis
(Todd), Gansserina cf. gansseri (Bolli), Globotruncana
arca (Cushman), G. arca-orientalis, G. dupeublei Caron
et al., G. esnehensis Nakkady, G. falsostuarti Sigal, G.
linneiana (d’Orbigny), G. mariei Banner & Blow, G.
orientalis El Naggar, G. ventricosa White, Globotruncanella
havanensis (Voorwijk), Globotruncanita angulata (Tilev),
G. conica (White), G. pettersi (Gandolfi), G. stuarti (de
Lapparent), G. stuartiformis (Dalbiez), Racemiguembelina
fructicosa (Egger), Rugoglobigerina rugosa (Plummer),
Praegublerina acuta (de Klasz) and Praegublerina robusta
(de Klasz) (Figure 6; Plate 1). The occurrence of A.
mayaroensis throughout the succession indicates that
age of the laminated micritic limestones in the Beytitepe
stratigraphic section is late Maastrichtian (Figures 3, 6).
The late Maastrichtian Abathomphalus mayaroensis is the

index species of the homonym biozone (Figure 3) (Bolli,
1957; Robaszynski et al. 1984; Caron 1985; Premoli Silva

147


SARI / Turkish J Earth Sci
21000

22000

23000

EXPLANATION

Bornovalı T.
51
61

78

sheared flysch
undifferentiated
Mesozoic blocks
(Işıklar Limestone)

84

nlık


Sa

D.

ka

yl
Ya

llı

nı

n

D

aba

.

ğla
r.
rı S

58

Berbersalih T.

upper Maastrichtian


70

Kara

Kocaçay Conglomerate
laminated
micritic
limestone

Beytitepe
Limestone

N

52000

36

unmapped area

51000

60

49

Kapuz D.

fault


32

24

52
45

50

79

62
65

puz

47

mi

42

kay

.

D.

.


stream

ası

.

kD

?
Beyti T.

33

Ovacık T.

Beytitepe MSS

26
25

rsi

45

nli

kD

49000


33

53

41

42

Gökdere
MSS

46

settlement

25

22

.

35

58

56

56


32

D.
61

43

Sivrikaya

Ayı
lı

40
38

measured stratigraphic
section (MSS) line

50

66

34
54

road
dirt tracts

49


30

Me

peak of hill
highway

.

64

strike and dip of
overturned bedding
axis of overturned
syncline

Ge

Gö

50
62

45

Çıtırlık T.

64

Ortaburun T.


22

75

D.

25
68

50000

strike and dip of bedding
vertical bedding

Ka

30

68

83

contact

Yaylaarkası T.

41

55

46

56
59
45

38

48000

49
70

pınar

Kara

Gökdere

D.

500 m

Figure 4. Geological map of the Gökdere area (See Figure 1b for location of the area).

& Sliter 1994; Sliter 1989; Premoli Silva & Sliter 1999;
Robaszynski et al. 2000; Premoli Silva & Verga 2004;
Sarı, 2006a, 2006b, 2009). The presence of C. contusa and
R. fructicosa also indicates a late Maastrichtian age. The
coexistence of the two species suggests the presence of

the C. contusa-R. fructicosa zone (Premoli Silva & Bolli
1973; Premoli Silva & Sliter 1994; Premoli Silva & Sliter
1999; Premoli Silva & Verga 2004), which corresponds to
the lowermost part of the late Maastrichtian (Figure 3).

148

In addition, G. conica, another late Maastrichtian species,
is also recorded throughout the section (Figure 6). These
data update the previous age assignment for these levels
(Campanian-Maastrichtian) by Erdoğan (1990b).
The Gökdere stratigraphic section A very thick pile of
laminated micritic limestones crops out just north of the
Gökdere Village. This increased thickness was caused by
an overturned syncline. Partial Bouma sequences were
observed in the sandstone-shale alternations to the SE and


SARI / Turkish J Earth Sci

sheared
flysch

230

220

FOSSIL EXPLANATION
echinoid


Fossil Symbol

Sample No
N-61
N-60
N-59
N-58
N-57
N-56
N-55

210
N-54
200

190

Fossil occurrences

N-44
N-43
N-42

170

N-41

160

N-40

N-39
N-37

150

N-36
N-35
N-34

140
N-33
130

relative abundance of a taxon

N-32
N-31
N-30

120

110

occurrence of a taxon

N-53
N-52
N-51
N-50
N-47

N-46
N-45

180

conglomerate
rudist-bearing
bioclastic limestone

Lithology

Thickness (m)

Unit

Stage

thin laminated
micritic limestone
laminated clayey
micritic limestone
laminated clayey limestone
with poor clay content
laminated micritic
limestone with sand to
block-size limestone clasts
calcareous shale
(with rich carbonate content)
calcareous shale
(with poor carbonate content)

flysch (sandstoneshale alternation)
sandstone bed with
erosive lower bed surface
(with partial Bouma sequences)
and sandstone lens

Beytitepe Limestone
upper Maastrichtian

BLOCKS

MATRIX

laminated micritic
limestone

Abathomphalus mayaroensis
Contusotruncana fornicata
Contusotruncana patelliformis
Globotruncana dupeublei
Globotruncanella havanensis
Globotruncanita stuarti
Globotruncanita stuartiformis
Gublerina sp.
Racemiguembelina fructicosa
Rugoglobigerina rugosa
Globotruncana linneiana
Globotruncanita conica
Contusotruncana contusa
Globotruncanita angulata

Globotruncana arca
Globotruncana ventricosa
Globotruncana esnehensis
Globotruncana mariei
Contusotruncana walfischensis
Globotruncana falsostuarti
Globotruncanita pettersi
Gansserina gansseri
Globotruncana arca-orientalis
Globotruncana orientalis

Planktic Foraminifera

EXPLANATION

N-29

100

N-28
N-27

90

N-26
N-25

probable occurrence of a taxon
80


Figure 5.
Lithology and fossil explanations for stratigraphic
sections.

70

60

NW of the micritic limestones. The position of the Bouma
sequences indicates that the SE flank of the fold is normal
and the NW flank is overturned (Figures 4, 8). The whole
limestone package was measured from SE to NW in order
to correlate the limestones with the Beytitepe stratigraphic
section. A 720 m thick limestone sequence was measured
through the section line. Hence, the thickness of the
laminated micritic limestones increases southwestwards
from 220 m to 360 m within 1 km (Figure 4). The body
of the laminated micritic limestones shows thickness
reduction from the Beytitepe measured section to the
NE and grades laterally into flysch-type rocks. Similarly,
a single body of the micritic limestones is separated into
several large and small lenses north of Beyti Tepe. They

N-24
N-23
N-22
N-21

50


N-20
N-19
N-18
N-17

40

30

20

N-16
N-15
N-13
N-12
N-10
N-9
N-8
N-7
N-6
N-5
N-4
N-3

10

sheared
flysch

N-2

N-1

Figure 6. Beytitepe stratigraphic section (See Figure 4 for
location of the section and Figure 5 for explanation).

149


SARI / Turkish J Earth Sci

a

b
planktic
foraminifera
cut by solution
seams
complete
planktic
foraminifera
shells

pressure
solution
seams

500 µm

c


d

500 µm

Figure 7. Field and photomicrographs of the laminated micritic limestones observed in the Gökdere area; (a) Close-up view of the
micritic limestones, which are mainly characterized by distinct lamination (Coordinate: 0520815/4248786). (b) Field photograph
of a Holasterid echinoid (probably Echinocorys) from the 149th metre of the Beytitepe stratigraphic section. (c) Photomicrograph of
laminated micritic limestones, which escaped the effect of shearing. Planktic foraminifera are observed as complete specimens within the
wackestone/mudstone microfacies (Sample no: N-3). (d) Photomicrograph of laminated micritic limestones, which contain numerous
pressure solution seams cutting planktic foraminifera embedded within the wackestone/mudstone microfacies (Sample no: N-28).

overturned flank
NW

N-227
X

normal flank
N-150
X

N-76
X

SE

250 m
sandstone beds with
partial Bouma sequences
Figure 8. Gökdere stratigraphic section. The section comprises

laminated micritic limestones within the flysch-type deposits,
which formed an overturned syncline. This section presents the
thickest package of laminated micritic limestones, which are
360-m-thick (See Figure 4 for location of the section).

150

interfinger with the flysch-type rocks and pinch out NE of
the study area (Figure 4).
The lithological, sedimentological and palaeontological
aspects of the micritic limestones of the Gökdere
stratigraphic section are similar to the limestones in the
Beytitepe stratigraphic section (Figure 8). One hundred
and fifty two limestone samples were collected for
thin section examination. The planktic foraminiferal
assemblages in the Gökdere stratigraphic section include all
the species observed in the Beytitepe stratigraphic section,
with, in addition, C. fornicata-patelliformis, C. plicata
(White), C. plummerae (Gandolfi), G. bulloides Vogler,
G. hilli Pessagno, G. insignis (Gandolfi), G. petaloidea
(Gandolfi), G. elevata (Brotzen), Radotruncana subspinosa
(Pessagno), Rugoglobigerina milamensis Smith & Pessagno,
Rugoglobigerina pennyi Brönnimann and biserial and
multiserial heterohelicids (See Plate 1 for the images). The
occurrence of A. mayaroensis indicates that the age of the


SARI / Turkish J Earth Sci

EXPLANATION


20000

Miocene

conglomerate
(Sabuncubeli Fm.)

unconformity

upper Maastrichtianupper Palaeocene

sheared flysch
undifferentiated
Late Cretaceous blocks
(Işıklar Limestone)

42

S-4

Beytitepe
Limestone

calcareous
shale
laminated
micritic
limestone
unmapped area

contact
covered contact
fault
strike and dip of bedding
vertical bedding

50

stream

.

S-2
S-3
67

46

35

.

ı
dağ

em

bad

Acı


52000

ak
D

.

S-2

peak of hill
section line and
section number

S-1

73

Ka

lab

22

20

N

36


250 m

Canavar T.

51000

20000

Figure 9. Geological map of the Işıklar area. Many lenses and blocks of the Beytitepe Limestone
seen at or close to matrix-block contact. (See Figure 1b for location of the area).

micritic limestones in the Gökdere stratigraphic section
is late Maastrichtian, as in the Beytitepe stratigraphic
section. Abathomphalus mayaroensis existed for 3.66 my
from 68.66 my to 65.0 my (Robaszynski 1998) (Figure 3).
During this time interval, a sequence at least 360 m thick,
made up of laminated micritic limestones, was deposited.
Therefore, the sedimentation rate of the laminated micritic
limestones was approximately 9.84 cm/ky. Because flyschtype sediments were observed at the base and top of the
limestones, the sedimentation rate obviously exceeded
9.84 cm/ky in this part of the basin.

4.2. The Işıklar area
Matrix and blocks of the BFZ were observed in the Işıklar
area (Figure 9). The contact between the matrix and the
blocks trends SW-NE and is mostly faulted. The matrix
consists mainly of sheared flysch, including laminated
micritic limestone and calcareous shale lenses in variable
thickness. These lenses occur mostly along or near the
block-matrix contact (Figure 9). The contacts between

the lenses and adjacent flysch deposits are generally sharp.
While original stratigraphic contact relations are generally
preserved, some micritic limestones have sheared contacts

151


upper
Palaeocene

upper
Maastrichtian

CampanianMaastrichtian

? Palaeocene

uppermost
CampanianMaastrichtain

Abathomphalus mayaroensis
Contusotruncana fornicata
Contusotruncana patelliformis
Contusotruncana plicata
Contusotruncana plummerae
Contusotruncana walfischensis
Globotruncana arca
Globotruncana dupeublei
Globotruncana linneiana
Globotruncana orientalis

Globotruncanella havanensis
Globotruncanita conica
Globotruncanita stuarti
Globotruncanita stuartiformis
Globotruncanita pettersi
Racemiguembelina fructicosa
Rugoglobigerina milamensis
Rugoglobigerina pennyi
Rugoglobigerina rugosa
Gublerina sp.
Multiserial heterohelicid
Globanomalina ehrenbergi
Globanomalina ehrenbergipseudomenardii
Globanomalina planoconica
Igorina albeari
Morozovella acuta
gr. M. angulata-M. aequa
Parasubbotina variospira
Globanomalina chapmani
Subbotina velascoensis
Globanomalina sp.

Figure 10. Section 1 is represented by many laminated micritic
limestone levels within the flysch and comprises many packages
separated by faults (See Figure 5 for explanation and Figure 9 for
location of the section).

with the flysch. 16 lenses and lensoid laminated micritic
limestone and calcareous shale blocks were sampled and
mapped. Although some lenses are a few metres thick,

they were indicated on the geological map exaggeratedly
as they contain important palaeontological data. 64
samples were collected from the Işıklar area. Laminated
micritic limestones are mostly light grey and similar to the
micritic limestones, somewhat as in the Gökdere area with
respect to lithological aspects, depositional texture and
planktic foraminiferal content. Some lenses have rather
poor planktic foraminifera content without any diagnostic
species. Therefore, four relevant sections are presented
here to save space;
Section 1 This section comprises several laminated
micritic limestone interlayers, which are intercalated
with flysch and separated by numerous faults (Figure
10). Sample N-268 yielded a rich planktic foraminiferal
assemblage. The occurrence of A. cf. mayaroensis in
the assemblage seemingly indicates that the age of the
laminated micritic limestone is late Maastrichtian. Other
late Maastrichtian species such as G. conica and R. fructicosa
were also observed in this sample (Figure 10; Plate 2).
Samples N-271 and N-273 include rare Maastrichtian
planktic foraminifera. The lenses from which samples
N-269, N-270 and N-272 were collected are similar to
the other lenses lithologically, but include late Palaeocene
planktic foraminifera such as Globanomalina cf. chapmani
(Parr), Globanomalina ehrenbergi (Bolli), Globanomalina
ehrenbergi-pseudomenardii, Globanomalina planoconica
(Subbotina), Igorina albeari (Cushman & Bermúdez),
Morozovella acuta (Toulmin), gr. Morozovella angulata
(White) - Morozovella aequa (Cushman & Renz),
Parasubbotina cf. variospira (Belford) and Subbotina

velascoensis (Cushman) (Figure 10; Plate 2). This section

152

X

1m

254

253
X

N-

X

W
1m

N-

NE

252

N-268

X


N-

X

251

N270

X

SW

N-

X

N269

N-

N271

3

27

X

N272


SARI / Turkish J Earth Sci

X

E

Globotruncana arca
Globotruncana dupeublei
Globotruncana falsostuarti
Globotruncana mariei
Globotruncanella havanensis
Globotruncanita conica
Globotruncanita stuarti
Globotruncanita stuartiformis
Racemiguembelina fructicosa
Multiserial heterohelicid
Globotruncana esnehensis
Globotruncanita pettersi
Globotruncana bulloides
Globotruncana linneiana

upper
Maastrichtian

Figure 11. Section 2 shows a 2-m-thick laminated micritic
limestone lens within the flysch (See Figure 5 for explanation and
Figure 9 for location of the section).

illustrates the magnitude of deformation that affected the
BFZ matrix, as lenses from various stratigraphic intervals

are in contact with each other (Figure 10).
Section 2 This section comprises a 2-m-thick
laminated micritic limestone interlayered within the flysch
sediments. The occurrence of G. conica and R. fructicosa
suggests a late Maastrichtian age (Figure 11; Plate 2).
Section 3 This section includes three laminated
micritic limestone levels. The lower two levels include
sand to block-size neritic and pelagic lithoclasts and
reworked benthic foraminifera, which are embedded
within a planktic foraminifera-bearing micrite matrix.
Sample N-264 was collected from the topmost level, and
its late Maastrichtian age is documented by the presence of
G. conica and R. fructicosa (Figure 12).
Section 4 This section comprises a beigish-grey to
pinkish-grey calcareous shale lens, which appears at
the matrix-block contact (Figure 9). The calcareous
shales gradationally overlie the flysch and include silt
to fine sand-size clasts at the base. Carbonate content
increases upwards. 12 samples were collected from the
calcareous shales (Figure 13), which mainly consist of
planktic foraminifera-bearing mudstones/wackestones
throughout (Figure 14). Planktic foraminifera assemblages
including Acarinina cf. strabocella (Loeblich & Tappan),
G. chapmani, G. compressa-ehrenbergi, G. ehrenbergi
(Bolli), G. cf. pseudomenardii (Bolli), I. albeari, I. pusilla
(Bolli), gr. M. angulata - M. aequa, Morozovella occlusa
(Loeblich & Tappan), Morozovella praeangulata-angulata,
P. variospira, S. triangularis (White) and S. velascoensis are
dominated by keeled Palaeocene forms, which became
dominant during the late Palaeocene (Olsson et al. 2011).

The occurrences of keeled Morozovella species such as gr.
M. angulata - M. aequa, M. occlusa and the other species
in the planktic foraminiferal assemblages, such as A. cf.


X

X

4m

X

Planktic Foraminifera

X

NW

X

X

X

X

SE

Figure 12. Section 3 shows three laminated micritic limestone

lenses. The uppermost level contains late Maastrichtian species.
(See Figure 5 for explanation and Figure 9 for location of the
section).

strabocella, G. chapmani, G. cf. pseudomenardii, I. albeari,
P. variospira and S. velascoensis (Figure 13; Plate 2) suggest
a late Palaeocene age (Berggren et al. 1995; Olsson et al.
1999; Berggren & Pearson 2005; Olsson et al. 2011). This
assemblage is documented for the first time from the
Işıklar area and provides important information about the
age of the matrix of the Bornova Flysch Zone. The only
palaeontologic data from that area were previosly recorded
by Özer & İrtem (1982), who identified a nannoplankton
assemblage and ‘Globoratalia sp.’, suggesting a Danian age.
4.3. The Kocaçay area
The geology of the Kocaçay area is rather complicated
(Figure 15) due to the presence of a large number of units
in such a small area, the blocky nature of the units and
syn-and post-depositional deformation. Also, contacts
of the units are generally concealed either because they
have soft lithologies, or by young cover and vegetation.
Despite the complexity of the geology and difficulties
mentioned above, the Kocaçay area displays important
information about the stratigraphy and the planktic
foraminiferal biostratigraphy of the matrix of the BFZ. The
data summarized below were based on detailed geological
mapping and measured stratigraphic sections. The matrix
and blocks of the BFZ were observed in the Kocaçay area.
Rudist-bearing neritic limestone blocks and planktic
foraminifera-bearing micritic limestone blocks were

observed within the pelagic laminated micritic limestones.
The original contact relations of the two lithologies were
also observed in this area. In many localities, rudist
fragments and benthic foraminifera-bearing neritic facies
is intercalated with the planktic foraminifera-bearing
pelagic facies. Field and thin section studies at these
levels revealed the allodapic nature of these deposits.
Occurrences of Dicarinella asymetrica (Sigal), Dicarinella
concavata (Brotzen) and Marginotruncana coronata (Bolli)
in pelagic facies indicate that the allodapic deposition
occurred during the middle-late Santonian. Blocks with
only pelagic or neritic facies were also identified. Small
and large (up to 250 m) laminated micritic limestone

Upper
Işıklar
Limestone Cret.

9

8

Sample No

Lithology

Thickness (m)

Stage


upper
Maastrichtian

upper Palaeocene

Maastrichtian

Beytitepe Limestone

Maastrichtian

Unit

1 m.

Globotruncana arca
Globotruncana linneiana
Globotruncanita pettersi
Globotruncana arca-orientalis
Globotruncana dupeublei
Globotruncana esnehensis
Globotruncana orientalis
Globotruncanita stuartiformis
Globotruncana bulloides
Globotruncanella havanensis
Globotruncanita conica
Globotruncanita stuarti
Racemiguembelina fructicosa
Rugoglobigerina pennyi
Rugoglobigerina rugosa

Gublerina sp.
Biserial heterohelicid
Multiserial heterohelicid

fault
N-242
N-241
N-240

7

N-239

6

N-238

5

Globanomalina ehrenbergi
Morozovella occlusa
Parasubbotina variospira
Acarinina strabocella
gr. M. angulata - M. aequa
Globanomalina chapmani
Globanomalina compressa-ehrenbergi
Globanomalina pseudomenardii
Igorina albeari
Igorina pusilla
Morozovella praeangulata-angulata

Subbotina triangularis
Subbotina velascoensis

X

N264

N260
N261
,26
2
N263

N257
N258

N255
N256

3m

N259

SARI / Turkish J Earth Sci

N-237
N-236

4
N-235

3
N-234
2

N-233

1

N-232

0

N-231

sheared
flysch

Figure 13. Section 4 was measured from a calcareous shale lens,
containing many keeled late Palaeocene planktic foraminifera.
(See Figure 5 for explanation and Figure 9 for location of the
section).

blocks are also present within the calcareous shales and the
Kocaçay Conglomerate (Figure 15).
The matrix of the BFZ in the Kocaçay area comprises
the Beytitepe Limestone, Kocaçay Conglomerate and
sheared flysch (Figures 2, 15). The Beytitepe Limestone
comprises two lithologies: laminated micritic limestones
and calcareous shales. Laminated micritic limestones
lie at the base of the matrix sequence in the Kocaçay

area. They include pelagic and neritic limestone blocks
of middle-late Santonian age in various sizes and shapes
(Figure 15). They are mostly grey or pale grey and include
pinkish grey, reddish grey and dark grey layers. Laminated
micritic limestones are mostly massive in appearance

153


SARI / Turkish J Earth Sci
21000

20000

34

14

20

250 m

keeled
late Palaeocene
planktic
foraminifera

N

21


S-8
62000

22

32

25
37

24
30

S-7

Ütük Tepe

26

?
ay D.

39

S-6

Kocaç

32


44

49

57

10
37

500 µm

30
78

EXPLANATION
34

36
12

46
34

154

BLOCKS

61000


sheared flysch
Kocaçay
Conglomerate
calcareous shale
laminated
micritic lmst.

up. Palaeoceneup. Maastricht.
up. Maastricht.
m-up. Santon.

pelagic limestone

Up. Cretaceous

neritic limestone
undifferentiated
blocks
unmapped area

55

21

10

contact
covered
contact
fault

covered
fault

50

Işıklar
Beytitepe
Limestone Limestone

terrace/recent cover

S-5

27

and bituminous. In thin section, they contain planktic
foraminifera-bearing mudstones/wackestones. Rarely,
reworked orbitoid benthic foraminifera fragments were also
observed within the micritic matrix. Planktic foraminifera
such as A. mayaroensis suggest a late Maastrichtian age.
Laminated micritic limestones are gradationally overlain
by calcareous shales, which are mainly red and reddish
to pinkish grey. The colour may change to pale greenishgrey. Sand to block-sized laminated micritic limestone
clasts were observed within the calcareous shales, which
mainly consist of abundant planktic foraminifera-bearing
wackestones to mudstones with a rare depositional
texture of planktic foraminifera. Planktic foraminifera
assocciations indicate a late Maastrichtian-late Palaeocene
age. Conglomerates cropping out in the Kocaçay area were
called the Kocaçay Conglomerate by Erdoğan (1990b).

The Kocaçay Conglomerate contains various pebble to
block-sized clasts from the underlying lithologies and
overlies the various stratigraphic levels of the laminated
micritic limestones and calcareous shales of the Beytitepe
Limestone. They also include laminated micritic limestone
blocks from pebble-size to 250 m across (Figure 15).
Sheared flysch cropping out in the westernmost part of
the study area overlies the conglomerates and consists of a
highly deformed sandstone-shale alternation. The sheared
flysch is the youngest level of the matrix of the BFZ in the
Kocaçay area.
One hundred and three samples were collected from
the laminated micritic limestones and the calcareous
shales of the Beytitepe Limestone and from several blocks
in order to understand the geology of the Kocaçay area, the
stratigraphy of the matrix and the planktic foraminiferal
biostratigraphy of the Beytitepe Limestone. Details of the
four selected stratigraphic sections are presented below
(Figures 16-19).
Section 5 Two lithologies of the Beytitepe Limestone are
overlain by Kocaçay Conglomerate in this section (Figure
16). Grey, locally pale reddish-grey laminated (massive

alluvium

61

MATRİX

Figure 14. Photomicrograph of the calcareous shales, represented

by the planktic foraminifera-bearing mudstone/wackestone
microfacies (Sample no: N-233).

strike and dip of
bedding
stream
road
section line

Figure 15. Geological map of the Kocaçay area. Four stratigraphic
sections were measured from the Beytitepe Limestone (See
Figure 1b for location of the area).

in appearance) bituminous micritic limestones lie at the
base of the sequence (Figure 20a). They are represented
by abundant planktic foraminifera, calcisphere and thin
shell fragments-bearing wackestones (Figure 20b). The
occurrence of A. mayaroensis in sample K-103 suggests
a late Maastrichtian age. In addition, occurrences of G.
conica, C. contusa and R. fructicosa from the samples
above the horizon with A. mayaroensis confirm this age
assignment (Figure 16; Plates 3, 4). Pinkish grey, distinctly
laminated calcareous shales overlie the laminated micritic
limestones along an uneven undulated surface (Figures
16, 20a). Calcareous shales fill the gaps in the laminated
micritic limestones through this uneven surface, which
is here interpreted as a block contact (Figure 20a).
The calcareous shales are represented by rich planktic
foraminiferal wackestones. Many pressure solution seams
were observed in thin sections. These surfaces cut many

planktic foraminifera, reducing the number of identifiable
species (Figure 20d). Occurrences of C. contusa and R.
fructicosa in the basal beds of the calcareous shales (samples
K-31, K-32) indicate a late Maastrichtian age (Figure 16;
Plates 3, 4). Towards the top is a thin calcareous shale
layer with rare planktic foraminiferal content, consisting
of mudstone with rare planktic foraminifera. The planktic
foraminifera are globular chambered small forms, which
are unidentifiable because they are cut by dissolution
surfaces. Cretaceous forms were not observed in this
level, and the small planktic foraminifera with globular
chambers could be Palaeocene species. Conglomerates


SARI / Turkish J Earth Sci

x K-29

N

cover
x

K-30
1m
section
line

x K-32
x


K-31

conglomerate
calcareous
shales
calcareous shales
laminated micritic
limestones
(massive in appearance)

K-34

x

a

x

x

K-35

K-33

K

K-100
X


K-101
X

2

KK- 29
30

4

x

x

K-102
X

-3

K

cover

-3

x

x

K


x

5

-3

-3

K

NW

K-103

SE

1

X

x

1m
x

K-33
Abathomphalus mayaroensis
Contusotruncana fornicata
Globotruncana bulloides

Multiserial heterohelicids
Gansserina gansseri
Globotruncana arca
Globotruncana dupeublei
Globotruncana hilli
Globotruncana orientalis
Globotruncanella havanensis
Globotruncanita pettersi
Globotruncana esnehensis
Globotruncana rosetta
Contusotruncana contusa
Contusotruncana walfischensis
Globotruncanita conica
Globotruncanita elevata
Globotruncanita stuarti
Globotruncanita stuartiformis
Globotruncana falsostuarti
Globotruncana linneiana
Globotruncana mariei
Racemiguembelina fructicosa
Radotruncana subspinosa
Globotruncana arca-orientalis
Rugoglobigerina rugosa
Biserial heterohelicids
Gublerina sp.
unidentified Paleocene species

b

?Palaeocene


upper Maastrichtian

Figure 16. Section 5; (a) Sketch map, (b) Cross section showing contact relations between the laminated micritic limestones and
calcareous shales of the Beytitepe Limestone and Kocaçay Conglomerate (See Figure 5 for explanation and Figure 15 for location of the
section).

155


SARI / Turkish J Earth Sci

Contusotruncana contusa
Globotruncana arca
Globotruncana dupeublei
Globotruncana esnehensis
Globotruncanita stuarti
Rugoglobigerina pennyi
Rugoglobigerina rugosa
Multiserial heterohelicids
Globotruncanita stuartiformis
Racemiguembelina fructicosa
unidentified Palaeocene species
Parasubbotina varianta
Subbotina velascoensis
Globanomalina compressa
Globanomalina planoconica
Subbotina triangularis

Sample No


Lithology

Thickness (m)

Unit
Stage

Planktic Foraminifera

Kocaçay
Conglomerate

34
K-86
32

uppermost Palaeocene

30
28

K-85
K-84
K-83
K-82

26
24


K-81
K-80

Beytitepe Limestone

K-79
22
K-78
20

K-77

18
K-76
16

upper Palaeocene

14

K-75

12

K-74

10

K-73


8

K-72
K-71

?lower Palaeocene

6
K-70
4
2

upper
Maast. 0

K-69
K-68
K-67
K-66
K-65

Figure 17. Section 6, showing details of the 35-m-thick calcareous
shales and overlying conglomerates (See Figure 5 for explanation
and Figure 15 for location of the section).

156

overlie the calcareous shales at the top of the succession
(Figure 16).
Section 6 A 35-m-thick sequence of calcareous

shales and overlying conglomerates was observed in
this section (Figure 17). The 1-m-thick basal part of the
calcareous shales is red and consists of abundant planktic
foraminiferal wackestones (Figure 20c, d), resembling the
calcareous shales observed in Section 5. Occurrences of
C. contusa and R. fructicosa in two samples (K-65, K-66)
suggest a late Maastrichtian age (Plates 3, 4). The overlying
calcareous shales are mainly red, but some thin beige-grey,
grey and pale greenish-grey layers were also observed.
Sand to block-size light grey bioclastic limestone clasts
were observed at some levels in the calcareous shales
(Figures 17, 20e). The first Palaeocene species appear
in sample K-67. The Palaeocene calcareous shales are
represented by a rare planktic foraminifer-bearing
mudstone depositional texture (Figure 20f). As many of
the species are cut by numerous pressure solution seams, it
is almost impossible to identify these species (Figure 20f).
Another difficulty in identifying the Palaeocene planktic
foraminifera in thin section is the frequent similarity of
axial sections of species of Subbotina, Parasubbotina and
Praemurica. For this reason, such species are grouped as
‘unidentified Palaeocene species’. However, it is possible
to identify some species such as P. varianta (Subbotina),
S. triangularis, S. cf. velascoensis, G. compressa (Plummer)
and G. planoconica (Figure 17; Plates 3, 4). The occurrence
of S. cf. velascoensis in sample K-70 suggests that this
level and the overlying 30 m thick calcareous shales were
deposited during the late Palaeocene (Olsson et al. 2011).
Morever, the occurrence of G. planoconica in sample K-77
indicates that the age of the 15 m thick uppermost part of

the calcareous shale sequence is latest Palaeocene (planktic
foraminiferal zones P4c to P5) according to Olsson et al.
2011 (Figure 3). Conglomerates overlie the calcareous
shales along a sharp contact in this section (Figure 17).
Section 7 In the northern part of the section, grey
bituminous micritic limestones containing thin shell
fragments lie at the base of the succession (Figure 18). In
the thin sections from samples K-20 and K-87 there are
very rare planktic foraminifera, reworked orbitoid benthic
foraminifera fragments, and an abundant microfacies
of wackestone containing recrystallized shell fragments.
A one metre thick, slightly recrystallized, indurated
laminated micritic limestone (massive in appearance) layer
overlies the micritic limestones. In thin section of samples
K-88, K-21 and K-89, a wackestone microfacies containing
abundant planktic foraminifera, rare calcisphere and shell
fragments was observed, as in the laminated micritic
limestones in Section 5. Laminated micritic limestones are
overlain by 4-m-thick red calcareous shales (Figure 18).
In thin sections of samples K-90, K-22, K-91 and K-92, a
rich planktic foraminifera-bearing depositional texture in
wackestone was observed, as in the red calcareous shales of
the Sections 5 and 6. The planktic foraminifera are diverse,
large, thick-walled and represented by morphologically
complex morphotypes (K-selection). Occurrences of A.


SARI / Turkish J Earth Sci

calcareous

shales

K-20

S

X

calcareous shales

X
X

fault
X

X

K-99

X

98

97
K-

96
X


K-

X

K-

X

95

94

conglomerates

K-

X

K-

KX

K-

K
K- -91
2 X
K
K -9 2 X
K- -89 0 X

K 21 X
K- -88 X X
87
X
N

92
93

calcareous shales with
rich carbonate content

laminated micritic limestones
bituminous micritic limestones

K-23

K-24

1m
Globotruncanita sp.
Orbitoid foraminifera
Abathomphalus mayaroensis
Contusotruncana contusa
Contusotruncana fornicata
Globotruncana dupeublei
Globotruncana esnehensis
Racemiguembelina fructicosa
Contusotruncana patelliformis
Globotruncanita angulata

Globotruncanita stuarti
Rugoglobigerina rugosa
Multiserial heterohelicids
Globotruncana arca
Globotruncanita conica
Globotruncanella havanensis
Rugoglobigerina milamensis
Contusotruncana plicata
Biserial heterohelicids
Gublerina sp.
Globotruncana mariei
unidentified ?Paleocene species
Globotruncanita insignis

upper
Maastrichtian

?Palaeocene

upper
Maastrichtian

Figure 18. Section 7, showing the stratigraphic relations of various lithologies of the Beytitepe
Limestone (See Figure 5 for explanation and Figure 15 for location of the section).

mayaroensis, C. contusa, G. conica and R. fructicosa at these
levels (Figure 18; Plates 3, 4) suggest a late Maastrichtian
age. Another upper Maastrichtian calcareous shale level,
which is overlain by conglomerates, was observed in the
southern part of the section (Figure 18). The colour of

the one meter thick uppermost layer of the calcareous
shales is pale greenish grey. Three lithologies seem to be
conformable, as a discontinuity surface was not observed
at the contacts. The presence of reworked orbitoid
benthic foraminifera, abundant shell fragments and the
scarceness of planktic foraminifera in the bituminous
micritic limestones indicate the proximity of the shallow
sea environment. Occurrences of planktic foraminifera,
together with calcispheres in laminated micritic limestones,
suggest a deeper depositional environment than in the
underlying orbitoid benthic foraminifera-bearing micritic
limestones. The abundance of the K-selected specialists
within the planktic foraminiferal assemblages in the red
calcareous shales means a deeper distal depositional
environment, as they dominate in open oceans, mainly
during the onset of highstands of sea level (Robaszynski
& Caron 1995). In summary, a deepening trend is clearly
seen from the micritic limestones to the calcareous shales
in the northern part of Section 7. Red calcareous shales
with very scarce planktic foraminifera occurring in mid-

section are similar to the Palaeocene calcareous shales in
Section 6.
Section 8 Calcareous shales, a laminated micritic
limestone block within the calcareous shales and overlying
conglomerates were observed in this section (Figure 19).
The laminated micritic limestone block is embedded
within the calcareous shale matrix and is very similar to
the laminated micritic limestones observed in Section
5. In thin section, they show a depositional texture

featuring planktic foraminifera, calcisphere and thin shell
fragments-bearing wackestone. Another small laminated
micritic limestone clast, 20 cm in diameter (sample K-59),
was observed within the calcareous shales (Figure 19).
Calcareous shales were observed beneath and above the
laminated micritic limestones and the contact between the
two lithologies is very similar to the contact in Section 5.
Calcareous shales fill the hollows in the laminated micritic
limestones with its uneven, undulating surface (Figure
19). Calcareous shales also resemble calcareous shales
observed in Sections 5, 6 and 7. Occurrences of rich late
Maastrichtian assemblages in both laminated micritic
limestones and calcareous shales indicates that laminated
micritic limestones were deposited, lithified, and then
subsequently fragmented and transported to the deeper
part of the basin during the late Maastrichtian.

157


SARI / Turkish J Earth Sci

laminated micritic
limestone block

section line

N

K-61

X

1m
X

X

K-59

K-60
K-37

X

K-57

X

K-56

K-58 X

X

Kocaçay
Conglomerate

calcareous shales
(Beytitepe Limestone)


slightly recristallized
laminated micritic limestones
(Beytitepe Limestone)

a
laminated micritic
limestone block

X

K-60
X

K-37
X

K-

K-61

59

NW
X

K-58
X

K-57 K-56
X

X

K-62
X

1m

SE

Globotruncana arca
Globotruncana bulloides
Globotruncana linneiana
Rugoglobigerina hexacamerata
Rugoglobigerina pennyi
Rugoglobigerina rugosa
Globotruncanella havanensis
Abathomphalus mayaroensis
Contusotruncana walfischensis
Globotruncana dupeublei
Globotruncana esnehensis
Globotruncana rosetta
Globotruncanita stuartiformis
Racemiguembelina fructicosa
Multiserial heterohelicids
Biserial heterohelicids
Contusotruncana contusa
Globotruncanita conica
Globotruncanita pettersi
Globotruncanita stuarti
Gublerina sp.

Contusotruncana patelliformis
Contusotruncana walfischensis
Globotruncana mariei

b

upper Maastrichtian

upper Maastrichtian

Figure 19. Section 8; (a) Sketch map, (b) Cross-section showing a late Maastrichtian laminated micritic
limestone block within late Maastrichtian calcareous shales (See Figure 5 for explanation and Figure 15 for
location of the section).

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block contact

sample numbers

planktic
foraminifers

calcisphere

calcareous shales
(Beytitepe Limestone)


shell fragments
laminated
micritic limestones
(Beytitepe Limestone)

a

b

500 µm

red calcareous shales
(Beytitepe Limestone)

pressure
solution
seams

X

K-66
thick-walled
planktic
foraminifers

c

X


K-65

d

globular-chambered
Palaeocene planktic
foraminifers

e

f

500 µm

pressure
solution
seams

500 µm

Figure 20. Field photographs and photomicrographs of the various lithologies of the Beytitepe Limestone in the Kocaçay area. (a)
Contact between the laminated micritic limestones and the calcareous shales. Numbers stand for sample numbers, which are indicated
in Section 5. (b) Photomicrograph of the laminated micritic limestones, represented by wackestones (Sample no: K-32 in Section 5), (c)
Close-up view of the upper Maastrichtian calcareous shales from Section 6 (Numbers stand for sample numbers, which are indicated in
Section 6), (d) Upper Maastrichtian calcareous shales are represented by abundant planktic foraminifera-bearing wackestones. The rock
and the planktic foraminifera are mostly cut by numerous pressure solution seams (Sample no: K-65 in Section-6), (e) Close-up view of
the upper Palaeocene calcareous shales (26.5th metre of Section 6, where sample K-82 was collected), (f) Palaeocene calcareous shales,
mainly represented by rare planktic foraminifera-bearing wackestones and mudstones. Pressure solution seams commonly cut planktic
foraminifera (Sample no: K-80 in Section-6).


159


SARI / Turkish J Earth Sci

STAGE
LITHOLOGY
MATRIX BLOCKS

LITHOLOGY
EXPLANATION

UNIT

highly sheared
sandstone-shale
alternation

sheared
flysch

conglomerate with
large limestone blocks

Kocaçay
Conglomerate

laminated micritic
limestone block


upper
Maast.

upperuppermost
Palaeocene

calcareous shale block

calcareous shale with
limestone block and pebbles

calcareous shale
laminated micritic
limestone block

upper
Maast.

Beytitepe
Limestone

laminated micritic
limestone

middle-upper
Santonian

upper Maastrichtian

?lower

Palaeocene

rudist-bearing
bioclastic limestone

Işıklar
micritic limestone with Limestone
planktic foramifers
laminated micritic
limestone

upper Maastrichtian

sandstone bed with
Bouma sequence
laminated micritic
limestone lens

Beytitepe
Limestone

laminated
micritic
limestone

Beytitepe
Limestone

conglomerate
lens

highly sheared
sandstone-shale
alternation
late Maastrichtian
planktic foraminifera

Palaeocene
planktic foraminifera

middle-late Santonian planktic foraminifera

sheared
flysch

Kocaçay
Conglomerate

late Palaeocene
planktic foraminifera

rudist

reworked orbitoid benthic foraminifera

Figure 21. Detailed stratigraphic column of the matrix of the Bornova Flysch Zone around Bornova. The column is based on data derived
from all three areas. The age of the Beytitepe Limestone and accompanying flysch-type rocks is late Maastrichtian in the Gökdere area
and late Maastrichtian and late Palaeocene in the Işıklar area. The age of the Beytitepe Limestone is late Maastrichtian-latest Palaeocene
in the Kocaçay area. The age of the Kocaçay Conglomerate and flysch, which overlie the calcareous shales must be latest Palaeocene or
younger.


160


SARI / Turkish J Earth Sci

5. Discussion and conclusions
Detailed studies based on the planktic foraminiferal
biostratigraphy of the Beytitepe Limestone in the matrix
of the BFZ around Bornova (İzmir) have revealed new
data about the stratigraphy and age of the matrix (Figure
21). The age of the laminated micritic limestones in the
Gökdere area, indicated by the occurrence of zonal maker
A. mayaroensis together with other late Maastrichtian
species such as C. contusa, G. conica and R. fructicosa,
is late Maastrichtian. The layer thickness attains 360 m,
indicating a sedimentation rate of at least 9.84 cm/ky. A
previous Campanian-Maastrichtian age assigned for this
level by Erdoğan (1990b) is revised in this study.
The Işıklar area has thin lenses of laminated micritic
limestones and calcareous shales within the flysch-type
deposits. A late Maastrichtian age was indicated for
the laminated micritic limestones by the presence of A.
mayaroensis, C. contusa, G. conica and R. fructicosa. A late
Palaeocene age was also documented from the calcareous
shale lenses, which contain an assemblage including many
keeled Morozovella species such as gr. M. angulata - M.
aequa, M. occlusa and other late Palaeocene species such
as A. cf. strabocella, G. chapmani, G. cf. pseudomenardii,
I. albeari, I. pusilla, P. variospira and S. velascoensis. Late
Maastrichtian and late Palaeocene ages are documented

for the first time in the Işıklar area by this study.
The Kocaçay area has a complicated geology and
provides important information about the stratigraphy
and age of the matrix of the BFZ. Laminated micritic
limestones are very similar to their counterparts observed
in the Gökdere and Işıklar areas. A late Maastrichtian age,
based on the occurrences of A. mayaroensis, C. contusa, G.
conica and R. fructicosa, was obtained from the laminated
micritic limestones, which are gradationally overlain by
the calcareous shales (Figure 21) which contain a rich late
Maastrichtian planktic foraminiferal assemblage. They
are dominated by diverse, large, thick-walled complex
morphotypes (K-selection), which indicate a deeper distal
depositional environment. The assemblage, including
A. mayaroensis, C. contusa, G. conica and R. fructicosa,
suggests a late Maastrichtian age. Blocks and pebbles of
the laminated micritic limestones were observed within

the calcareous shales, which are overlain by Palaeocene
calcareous shales (Figure 21). The Late Maastrichtian and
Palaeocene calcareous shales are similar in appearance but
the Palaeocene calcareous shales have a scarce planktic
foraminifera content. Poor assemblages, including P.
varianta, S. triangularis, S. cf. velascoensis, G. compressa
and G. planoconica, indicate a late Palaeocene age for the
lower part and a latest Palaeocene age for the upper part of
the calcareous shale sequence. In this study, index species
such as A. mayaroensis, G. conica, R. fructicosa and many
other Maastrichtian species have been documented from
this area for the first time. It appears that the age of the

calcareous shales extends to the latest Palaeocene, which
is also new information about this area (Figure 21). The
Kocaçay Conglomerate overlies various stratigraphic
levels of the calcareous shales and laminated micritic
limestones (Figure 21). Flysch-type sediments are the
younger lithologies in the Kocaçay area and overlie the
Kocaçay Conglomerate (Figure 21).
Based on the palaeontological data from the planktic
foraminifera from all three areas, it can be concluded that
the age of the Beytitepe Limestone and accompanying
flysch-type sediments is late Maastrichtian in the Gökdere
area, late Maastrichtian and late Palaeocene in the Işıklar
area and late Maastrichtian - latest Palaeocene in the
Kocaçay area. The age of the Kocaçay Conglomerate and
overlying flysch-type deposits in the Kocaçay area must be
latest Palaeocene or younger (Figure 21).
Acknowledgements
This study was financially supported by a TUBİTAK grant
109Y182 and Dokuz Eylül University (BAP) grant 2009.
KB.FEN.064, which are gratefully acknowledged. Dan
Georgescu and an anonymous reviewer are thanked for
their valuable constructive reviews. The help of Atilla
Kandemir and Ömer Ilgın during the field studies is
appreciated. I also would like to thank Taner Korkmaz
for participating in the field studies and for his help in
drawing some of the figures. I would like to thank Maria
Rose Petrizzo for valuable comments of some planktic
foraminifera identifications, especially the Palaeocene
species.


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Plate 1
Planktic foraminifera observed in the Gökdere area.
1. Abathomphalus mayaroensis (Bolli), Sample no: N-44,
2. Abathomphalus mayaroensis (Bolli), Sample no: N-90,
3. Abathomphalus mayaroensis (Bolli), Sample no: N-16
4. Contusotruncana contusa (Cushman), Sample no: N-17
5. Contusotruncana fornicata (Plummer), Sample no: N-130
6. Contusotruncana fornicata-patelliformis, Sample no: N-116
7. Contusotruncana patelliformis (Gandolfi), Sample no: N-102
8. Contusotruncana walfischensis (Todd), Sample no: N-92
9. Gansserina cf. gansseri (Bolli), Sample no: N-53
10. Globotruncana arca (Cushman), Sample no: N-38
11. Globotruncana arca-orientalis, Sample no: N-97
12. Globotruncana bulloides Vogler, Sample no: N-206
13. Globotruncana stuarti (de Lapparent), Sample no: N-110
14. Globotruncana esnehensis Nakkady, Sample no: N-81
15. Globotruncana cf. falsostuarti Sigal, Sample no: N-193
16. Globotruncana hilli Pessagno, Sample no: N-211
17. Globotruncana linneiana (d’Orbigny), Sample no: N-101
18. Globotruncana ventricosa White, Sample no: N-42

19. Globotruncanella havanensis (Voorwijk), Sample no: N-102
20. Globotruncanita conica (White), Sample no: N-20
21. Globotruncanita elevata (Brotzen), Sample no: N-99
22. Globotruncanita pettersi (Gandolfi), Sample no: N-193
23. Racemiguembelina fructicosa (Egger), Sample no: N-17
24. Rugoglobigerina milamensis Smith & Pessagno, Sample no: N-116
25. Rugoglobigerina pennyi Brönnimann, Sample no: N-52
26. Rugoglobigerina rugosa (Plummer), Sample no: N-212
27. Praegublerina acuta (de Klasz), Sample no: N-227
28. Multiserial heterohelicids, Sample no: N-101
29. Praegublerina robusta (de Klasz), Sample no: N-111

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Plate 2
Planktic foraminifera observed in the Işıklar area.
1. Acarinina cf. strabocella (Loeblich & Tappan), Sample no: N-234,
2. Globanomalina chapmani (Parr), Sample no: N-245,
3. Globanomalina chapmani (Parr), Sample no: N-232,
4. Globanomalina ehrenbergi (Bolli), Sample no: N-232,
5. Igorina albeari (Cushman & Bermúdez), Sample no: N-232,
6. gr. Morozovella angulata (White) - Morozovella aequa (Cushman & Renz), Sample no: N-232,
7. Morozovella acutispira (Bolli & Cita), Sample no: N-275,
8. gr. Morozovella angulata (White) - Morozovella aequa (Cushman & Renz), Sample no: N-233,
9. Globanomalina cf. pseudomenardii (Bolli), Sample no: N-236,
10. Globanomalina planoconica (Subbotina), Sample no: N-269,
11. Igorina albeari (Cushman & Bermúdez), Sample no: N-245,

12. Acarinina cf. strabocella (Loeblich & Tappan), Sample no: N-231,
13. gr. Morozovella conicotruncana (Subbotina) - Morozovella velascoensis (Cushman), Sample no: N-245,
14. Subbotina triangularis (White), Sample no: N-234,
15. Parasubbotina variospira (Belford), Sample no: N-231,
16. Subbotina velascoensis (Cushman), Sample no: N-245,
17. Contusotruncana plicata (White), Sample no: N-268,
18. Contusotruncana walfischensis (Todd), Sample no: N-268,
19. Globotruncana arca (Cushman), Sample no: N-268,
20. Globotruncana dupeublei (Caron et al.), Sample no: N-252,
21. Globotruncana linneiana (d’Orbigny), Sample no: N-249,
22. Globotruncana mariei Banner & Blow, Sample no: N-251,
23. Globotruncana orientalis El Naggar, Sample no: N-268,
24. Globotruncanella havanensis (Voorwijk), Sample no: N-268,
25. Globotruncanita stuarti (de Lapparent), Sample no: N-251,
26. Globotruncanita pettersi (Gandolfi), Sample no: N-268,
27. Rugoglobigerina hexacamerata Brönnimann, Sample no: N-246,
28. Rugoglobigerina milamensis Smith & Pessagno, Sample no: N-268,
29. Racemiguembelina fructicosa (Egger), Sample no: N-268,
30. Multiserial heterohelicids, Sample no: N-251,

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500 µm
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