GeolCarp_Vol58_No1_41

GEOLOGICA CARPATHICA, FEBRUARY 2007, 58, 1, 41—52

www.geologicacarpathica.sk

Biostratigraphy and paleoenvironmental interpretation of

the Middle Miocene submarine fan in the Adana Basin

(southern Turkey)

HURùYE DEMùRCAN

and AY EGÜL YILDIZ

General Directorate of Mineral Research and Exploration, Natural History Museum, 06520 Balgat, Ankara, Turkey;

huriyedemircan@yahoo.com

Aksaray University, Engineering Faculty, Department of Geological Engineering, 68100 Aksaray, Turkey; ayildiz@nigde.edu.tr

(Manuscript received November 18, 2005; accepted in revised form June 19, 2006)

Abstract:  The  turbiditic  Cingöz  Formation  of  the  Karaisah-Çatalan-Eûner  region,  Adana  Basin,  southern  Turkey  was
studied in detail in two sections based on planktonic foraminifers, calcareous nannofossils and trace fossils. The Middle
Miocene  (Langhian—Serravalian)  age  of  the  sediments  is  supported  by  the  Praeorbulina  glomerosa  curva  and  Orbulina
suturalis  planktonic  foraminiferal  Zones  and  by  standard  nannoplankton  Zones  NN5  Sphenolithus  heteromorphus  and
NN6 Discoaster exilis. Moreover, 24 ichnotaxa were identified and attributed to the Skolithos-Cruziana, mixed (Skolithos-
Cruziana and Nereites), and Nereites ichnofacies. Fossil assemblages indicate eutrophic and oligotrophic conditions. In the
Langhian,  the  distribution  and  percentage  abundances  of  temperature  sensitive  planktonic  taxa  including  Globigerina
falconensis  reflect  temperate  to  cold  surface  waters  in  the  depositional  area  of  the  western  and  eastern  fans  of  Cingöz
Formation. In Serravalian, higher numbers of warm-water prefering taxa indicate the rise in temperature in the western fan.

Key words: Middle Miocene, southern Turkey, biostratigraphy, paleoenvironmental interpretation, calcareous
nannoplankton, planktonic foraminifers, trace fossils, ichnofacies.

Introduction

The  Cingöz  submarine  fan  system  is  located  approxi-
mately  fifty  km  north  of  Adana  in  1 : 100,000  Kozan  N34
Sheet  in  the  northern  part  of  the  Adana  Basin  (Fig. 1).
The  following  studies  on  the  studied  region  and  closed

areas  have  been  published:  Schmidt  (1961),  Özgül  et  al.
(1972, 1973),  Yeti   &  Demirkol  (1984)  studies  about  the
stratigraphic  properties  of  the  area;  Görür  (1980),  Erten
(1983),  Yalçôn  &  Görür  (1984),  Yeti   et  al.  (1986),
Gökçen  et  al.  (1987),  Naz  &  Çuhadar  (1988),  Ünlügenç
et  al.  (1993),  Gürbüz  (1998)  studies  about  the  sedimen-

Fig. 1. Geological sketch map and the position of the investigated sections (after Gürbüz 1993 modified).

DEMùRCAN and YILDIZ

tology of the area; Nazik & Toker (1986), Toker & Yôldôz
(1991), Ünlügenç &

afak (1992), Nazik & Gürbüz

(1992),  Toker  et  al.  (1996),  Akça  et  al.  (1998),  Yôldôz  et  al.
(2003)  studies  about  the  paleontology;  Uchman  &  Demir-
can  (1999a,b),  Uchman  et  al.  (2002),  Demircan  &  Toker
(2003,  2004)  dealt  with  trace  fossils;  Özgül  (1976),  en-
gör  et  al.  (1985),  Gökçen  et  al.  (1988)  studies  concentrated
on  the  plate  tectonic  evolution  of  the  area  and  vicinity
while  Ketin  (1966)  and  Ayhan  (1978)  studies  concentrat-
ed  on  the  general  geology.

The purpose of this study is to present the planktonic

foraminiferal  and  calcareous  nannoplankton  biostratigra-
phy  of  the  Cingöz  Formation,  to  evaluate  depositional
environments  on  the  basis  of  trace  fossil  assemblages,
and  to  determine  changes  in  paleotemperature  of  the  sea-
surface  water  in  the  region  during  the  Middle  Miocene
based  on  abundance  and  distribution  of  temperature-sensi-
tive  planktonic  foraminiferal  and  calcareous  nannoplank-
ton  species.

Material and method

The material for this study comprised 30 samples col-

lected  from  two  sections  –  Kalaycôlar  (western  fan)  and
Ku çusofulu  (eastern  fan)  (Fig. 1).  The  numbers  of  speci-
mens  of  different  species  of  planktonic  foraminifers  in
100 g  of  washed  sample  were  recorded  as  abundant,  60—100
specimens;  common,  30—60  specimens;  few,  10—30  speci-
mens;  and  rare  1—10  specimens.  For  the  analysis  of  calcar-
eous  nannoplankton,  smear  slides  were  prepared  from  raw
(untreated)  samples.  No  specific  techniques  were  applied
to  clean  or  concentrate  the  biogenic  fraction,  the  aim  be-
ing  to  maintain  the  original  composition  of  the  nannofos-
sil  assemblages.  Smear  slides  were  examined  under  an
Ortholux  polarizing  microscope  using  an  oil-immersion
objective  of

100. Nannofossil abundances were estimat-

ed  using  the  scheme  of  Wei  (1988).  Based  on  this  method,
one  or  more  specimens  of  a  taxon  in  each  field  of  view  was
abundant,  one  specimen  of  a  taxon  in  2—10  fields  of  view
was  common,  one  specimen  of  a  taxon  in  11—50  fields  of
view  was  nominated  as  a  few,  and  one  specimen  of  a  taxon
per  51—200  fields  of  view  was  accepted  as  rare.

In this paper the planktonic foraminiferal zonations of

Jenkins  (1985)  (Southern  mid-latitude),  Iaccarino  (1985)
(Mediterranean),  Krasheninnikov  &  Kaleda  (1994)  (South-
ern  Cyprus),  and  Berggren  et  al.  (1995)  (Subtropical)  and
the  calcareous  nannoplankton  zones  of  Martini  (1971)
and  Perch-Nielsen  (1985)  were  used  for  biostratigraphic
interpretations.  In  addition,  the  abundance  (%)  and  distri-
bution  of  temperature-sensitive  planktonic  foraminiferal
and  calcareous  nannoplankton  species  in  each  sample
were  determined  for  the  next  paleoenvironmental  interpre-
tations.

Trace fossil studies were concentrated on the various

lithologies  represented  in  the  two  sections.  Trace  fossils  in-
vestigations  were  carried  out  both  on  bedding  and  parting
surfaces  of  sections  and  photographed  when  necessary.  Ich-
nofacies  interpretation  was  done  by  Seilacher  (1967).

Geological setting and sedimentology of the Cingöz

Formation

Two major sedimentary basins (Antalya and Çukurova)

existed  in  the  Late  Cenozoic  epoch  in  the  southern  Tur-
key  (Kelling  et  al.  1987).  The  Çukurova  Basin  Complex
comprises  the  Adana  and  Iskenderun  Sub-Basins  separated
by  the  Misis  Structural  High  Complex,  which  is  bounded
by  the  Ecemi   fault  in  the  west,  the  Tauride  Orogenic  Belt
in  the  north  and  the  Amanos  Mountains  in  the  east.  In  the
study  area,  Yeti   &  Demirkol  (1986),  and  Gürbüz  &
Kelling  (1991),  have  undertaken  sedimentological  inves-
tigation  of  the  Cingöz  Formation.  These  authors  conclud-
ed  that  the  formation  was  deposited  in  a  basin  plain  and
built  by  distal  and  proximal  portions  of  submarine  fans.
The  deep  marine  turbiditic  sandstone  systems  of  Middle
Miocene  age  were  formed  in  the  northern  part  of  the
Adana  Basin  as  two  (western  and  eastern)  deep-sea  fans.
The  western  fan  derived  from  the  northwest,  whereas  the
eastern  fan  was  supplied  from  the  north  (Fig. 1).  These  are
small,  ‘classical’,  sand-rich  submarine  fans  as  defined  by
Mutti  (1985)  and  Mutti  &  Normak  (1987).

Western fan

The western fan consists of two megacycles: lower se-

quence  and  upper  lobe-dominated  succession  dominated
by  coarse-  to  fine-grained  sandstone,  upwards  gradually
passing  into  the  outer  fan/basin  plain  sediment.  The  lobe
and  channel  deposits  are  attached  physically,  both  lateral-
ly  and  vertically.  No  clear  distinction  between  the  lower,
middle  and  upper  fan  elements  are  observed  in  the  field
because  of  the  attached  geometry.  The  maximum  thick-
ness  of  the  fan  is  around  1500 m  and  corresponds  well  to
the  low  efficiency  or  type II  turbidite  system  sensu  Mutti
(1985)  (Gürbüz  1993).

Eastern fan

The eastern submarine fan system was initiated by the

incision  of  individual  proximal  fan  channels  that  were
probably  physically  linked  to  major  channels  cut  into
shallow  marine  sediments  to  the  north,  permitting  the  ‘by
passing’  of  coarse  sediments  through  the  mixed  carbonate-
siliciclastic  marginal  facies  belt.  The  lower  part  of  this
body  starts  with  isolated  channels  and  is  less  conglomerat-
ic  than  the  western  body,  with  maximum  clast  sizes
around  60 cm.  The  thickness  of  this  basal  sequence  is
around  500 m.  The  second  phase  of  this  eastern  submarine
fan  starts  with  a  sequence  of  small  isolated  channels.
These  are  followed  by  a  succession  of  prograding  lobe-
dominated  mid-fan  cycles  with  thick,  coarsening  and
thickening  upward  cycles  of  sandstone  beds.  Thin-bedded
sandstone  beds  characterize  the  upper  part  of  the  eastern
fan  sequence  and  shale  intercalations  belong  to  the  lower
fan/basin  environment.  The  channels  and  the  lobes  in  the
lower  part  of  phase 2  sequences  are  detached  physically,
but  the  overlying  lobes  are  generally  mutually  attached.
The  eastern  fan  is  more  complex,  laterally  extensive  and

BIOSTRATIGRAPHY OF THE MIOCENE SUBMARINE FAN (SOUTHERN TURKEY)

thicker (approximately 3000 m maximum) than
the western body (Gürbüz 1993).

Results

Sediments of the Kalaycôlar and Ku çusofulu

sections  (see  Fig. 1),  provided  rare  but  well  pre-
served  tests  of  planktonic  foraminifers  and  medi-
um  well  preserved  calcareous  nannofossils.  The
foraminiferal  assemblages  are  composed  of  11
species  of  6  genera,  and  the  nannofossil  associa-
tions  are  composed  of  27  species  of  10  genera.
Some  taxa  and  abundance  differences  were  re-
corded  in  both  sections.

Kalayc

ôôôôô lar section, western fan of the Cingöz

Formation

Foraminifers (Fig. 3)

The lower part of the section (samples 1—5,

Fig. 2)  is  characterized  by  abundances  of  species
Praeorbulina  glomerosa  curva,  Globigerinoides
bisphericus,  G.  trilobus,  and    Globoquadrina
dehiscens.  Tests  of  Globigerina  falconensis
form  2—6 %  of  the  assemblage.  In  the  upper  part
of  the  section  (samples  6—14)  specimens  of  Orbu-
lina  suturalis  and  O.  bilobata  were  recorded  ac-
companied  by  higher  numbers  of  Globigerinoides
trilobus,  Globoquadrina  altispira  conica,  and  G.
dehiscens.  The  abundance  of  Globigerina  falcon-
ensis  falls,  forming  about  1—2 %  of  assemblage.
Specimens  of  P.  glomerosa  curva  have  not  been
already  recorded  (see  Fig. 2).

Calcareous nannoplankton (Fig. 4)

Samples 1—7 (see Fig. 2) contain rare Spheno-

lithus  heteromorphus  and  higher  numbers  of  Coc-
colithus  miopelagicus  and  Sphenolithus  abies.
The  upper  part  of  the  section  (samples 8—14)  is
characterized  by  abundance  of  Reticulofenestra
pseudoumbilica  (recorded  first  in  sample  No. 8)
and  by  higher  numbers  of  Discoaster  aulakos,  D.
variabilis  and  Coccolithus  miopelagicus  (Fig. 2).
Concerning  sphenoliths,  S.  abies  occurs  up  to  the
sample  No. 9  and  S.  heteromorphus  is  already  ab-
sent  in  this  interval.  Rare  specimens  of  Braaru-
dosphaera  bigelowii  were  observed  through  the
whole  profile.

Ku çusofulu section, eastern fan of the Cingöz
Formation

Foraminifers (Fig. 3)

Lower part of section (samples 1—7, Fig. 5) con-

tained abundant specimens of Praeorbulina glome-

Fig. 2.

Kalayc

ôlar

section,

western

fan

the

Cingöz

ormation.

Distribution

lanktonic

foraminifers,

calcareous

annofossils

and

trace

fossils

and

their

biostratigraphic

interpretation

including

percentage

Globigerina

falconensis

and

temperature

sensitive

nannoplankton

taxa.

DEMùRCAN and YILDIZ

rosa  curva,  Globigerinoides  bisphericus,  G.  trilobus,  and
Globoquadrina  dehiscens.  The  upper  part  of  the  section
(samples 8—16)  is  characterized  by  the  occurrence  of  Orbu-
lina  suturalis  and  O.  bilobata  and  by  higher  numbers  of
Globigerinoides  trilobus,  Globoquadrina  altispira  conica,
and  G.  dehiscens.  Species  P.  glomerosa  curva  has  not  been
found  here.  Abundance  of  Globigerina  falconensis  varies
between  2—6 %  during  the  whole  section  (see  Fig. 5).

Calcareous nannoplankton (Fig. 4)

The lower part of the fan (samples 1—10) is characterized

by  the  presence  of  Sphenolithus  heteromorphus  and  S.
abies  and  by  high  numbers  of  Coccolithus  miopelagicus,
Reticulofenestra  pseudoumbilica  and  Helicosphaera  phil-
ippinensis.  In  the  overlying  strata  (samples  No. 11—16)  the
occurrence  of  other  taxa  was  recorded,  such  as  Dictyococ-
cites  productus,  Coronocylus  nitescens,  Helicosphaera
orientalis,  and  others  (see  Fig. 5).  The  assemblages  con-
tain  abundant  specimens  of  Coccolithus  miopelagicus
and  Reticulofenestra  pseudoumbilica.  The  stratigraphical-
ly  important  species  Sphenolithus  heteromorphus  and  S.
abies  have  not  been  recorded.  Rare  specimens  of  Braaru-
dosphaera  bigelowii  were  observed  through  the  whole
profile.

Trace fossils

Twenty-four ichnotaxa have been recognized in the in-

vestigated area. Trace fossils have been observed on bed-

ding  and  on  parting  surfaces  and  in  vertical  sections.  The
following  trace  fossil  assemblages  were  determined  in
the  Cingöz  Formation  western  fan  –  from  the  lower  part
of  the  section  to  the  top:  Ophiomorpha  isp.,  Thalassi-
noides  isp.,  Skolithos  isp.,  Chondrites  isp.,  Scolicia  isp.,
Planolites  isp.,  Scolicia  vertebralis,  Phycodes  isp.,  Zoo-
phycos  isp.,  Capodistria  vettersi,  Halopoa  annulata,
Helminthopsis  isp.,  and  Cosmorhaphe  sinuosa.  In  the
lower  part  of  the  eastern  fan  to  the  top:  Ophiomorpha
isp.,  Ophiomorpha  annulata,  Thalassinoides  isp.,  Ha-
lopoa  annulata,  Lophoctenium  isp.,  Phymatoderma  isp.,
Nereites  isp.,  Nereites  irregularis,  Paleodictyon  isp.,  Pa-
leodictyon  delicatulum,  and  Paleodictyon  majus.  Distri-
bution  of  most  of  the  described  trace  fossils  does  not
show  any  distinct  rules.  Only,  Scolicia  vertebralis  and
Echinospira  isp.,  display  a  tendency  to  occur  in  the
thicker  beds.  Ophiomorpha  and  Thalassinoides  isp.  only
occur  in  thicker  beds.  The  remaining  ichnotaxa  are  sepa-
rated  more  or  less  in  thinner  beds.  The  described  trace
fossil  assemblage  is  dominated  by  ichnotaxa  of  the  Nere-
ites  ichnofacies,  represented  by  meandering  pascichnia
(Nereites,  Scolicia)  and  different  graphoglyptids  (e.g.
Paleodictyon  isp.,  Desmograpton  isp.,  Cosmorhaphe
isp.,  Helminthorhaphe  isp.).  Stationary  fodichnia  (Echi-
nospira  isp.)  and  ?chemichnia/fodichnia  (Chondrites
isp.)  also  occur  there.  ‘Shallow-water’  vertical  forms
(horn-like  form  and  Ophiomorpha  isp.)  typical  of  the
Skolithos  ichnofacies,  and  Thalassinoides,  which  is  the
most  characteristic  of  the  Cruziana  ichnofacies,  are
present there (Figs. 2, 5, 8, 9).

Fig. 3. a – Globigerinoides bisphericus, Kalaycôlar section, Sample KC-2; b – Globigerinoides trilobus, Ku çusofulu section, Sample
KS-4; c – Globigerinoides trilobus, Ku çusofulu section, Sample KS-16; d – Praeorbulina glomerosa curva, Ku çusofulu section,
Sample KS-3; e – Orbulina suturalis, Ku çusofulu section, Sample KS-10; f – Globoquadrina dehiscens, Kalaycôlar section, Sample KC-5;
g – Globoquadrina dehiscens, Kalaycôlar section, Sample KC-3; h – Globigerina woodi connecta, Kalaycôlar section, Sample KC-5.

DEMùRCAN and YILDIZ

Fig.

Kuçusofulu

section,

eastern

fan

the

Cingöz

Formation.

Dist

ribution

planktonic

foraminifers,

calcareous

nannofossils

trace

fossils

and

their

biostratigraphic

interpretation

in-

cluding

percentage

Globigerina

falconensis

and

temperature

sensitive

nannoplankton

taxa.

Biostratigraphy

According to the presence of the for-

aminiferal  species  Praeorbulina  glom-
erosa  curva,  the  sediments  from  the
localities  Kalaycôlar,  western  fan  (sam-
ples 1—5,

Fig. 2)

and

Ku çusofulu,

eastern fan (samples 1—7, Fig. 5) are
correlated

with

Zone

Praeorbulina

glomerosa curva (sensu Jenkins 1985;
Iaccarino

1985;

Krasheninnikov

Kaleda  1994;  Berggren  et  al.  1995)
(Fig.  6).  This  interval  is  also  defined  as
the  Praeorbulina  glomerosa  s.s.  Zone
in  subtropical  areas  (Berggren  et  al.
1995),  Mediterranean  (Iaccarino  1985)
and  Southern  Cyprus  (Krasheninnikov
&  Kaleda  1994)  and  as  the  Praeorbu-
lina  glomerosa  curva  Zone  in  south-
ern

mid-latitudes

(Jenkins

1985).

Zone  Praeorbulina  glomerosa  curva
is  attributed  to  the  Langhian  Stage
(16.1—15.1 Ma)  (Berggren  et  al.  1995).
In  the  studied  material,  this  interval  is
correlated  with  nannoplankton  Zone
NN5  (Martini  1971;  Perch-Nielsen
1985)  (Fig.  7)  according  to  the  presence
of  the  species  Sphenolithus  heteromor-
phus  and  absence  of  Helicosphaera  am-
pliaperta  (see  Figs. 2  and  5).

The foraminiferal species Orbulina

suturalis  and  O.  bilobata  (Kalaycôlar,
samples 6—14,  Fig. 2  and  Ku çusofulu,
samples  8—16,  Fig. 5)  indicate  Zone  Or-
bulina  suturalis  (Jenkins  1985;  Iaccari-
no  1985)  that  is  correlated  with  the
upper  part  of  Langhian  Stage  and  with
the  Serravalian  (15.1—12.7 Ma).  The
presence  of  Sphenolithus  heteromor-
phus  in  the  sections  of  Kalaycôlar  (sam-
ples 6,  7,  Fig. 2)  and  Ku çusofulu
(samples 8—10,  Fig. 5)  gives  evidence
for  the  standard  nannoplankton  Zone
NN5  and  its  absence  in  the  overlying
strata  may  indicate  Zone  NN6.

Paleoenvironmental

interpretations

The foraminiferal species Globigeri-

na  falconensis  is  a  temperature  sensi-
tive  taxon  and  its  presence  reflects  cold
to  subtropical  water  conditions  (water
temperature  2—20 ºC)  (Parker  &  Berger
1971;  Thunell  1977;  Cullen  &  Prell
1984).

Distribution

and

percentage

abundances of G. falconensis in the
western and eastern fans of Cingöz For-

BIOSTRATIGRAPHY OF THE MIOCENE SUBMARINE FAN (SOUTHERN TURKEY)

mation  varies  between  1—6 %  (see  Figs. 2  and  5),  so,  pres-
ence  of  this  species  indicates  temperate  to  cold  sea  surface
waters.  The  locality  Kalaycôlar,  western  fan  of  the  Cingöz
Formation  in  an  exception.  The  numbers  of  G.  falconensis
fall  to  about  1—2 %  of  assemblage  during  Serravalian  (see
Figs. 2  and  5).  This  phenomenon  may  indicate  input  of
warm waters.

Concerning calcareous nannoflora, higher numbers

(22—95 %)  of  Coccolithus  miopelagicus,  C.  pelagicus,
Reticulofenestra  pseudoumbilica  and  R.  haqii  support
temperate  to  cold  water  conditions  (McIntyre  et  al.  1970;
Bukry  1973;  Siesser  &  Haq  1987;  Wei  &  Wise  1989)
whereas  species  that  are  mentioned  as  tropical  to  temper-
ate  latitude  taxa,  such  as  genera  Discoaster,  Spheno-
lithus

and

Helicosphaera

form

ca.

5—55 %

assemblage.  The  exception  is  the  Serravalian  deposits  at
the  locality  of  Kalaycôlar,  western  fan  that  provided
higher  numbers  of  tropical  to  temperate  latitude  nanno-
fossils  with  increasing  percentages  from  30  to  50—55 %
and  decreasing  numbers  of  temperate  to  high-latitude
taxa  (25—30 %).  These  observations  support  the  theory
that  the  sea-surface  waters  were  relatively  cold  in  the
depositional  area  of  the  Cingöz  Formation  in  the  Lang-
hian  but  during  the  Serravalian  the  sea-surface  waters
were  getting  warm  especially  in  the  area  of  the  western
fan.  It  was  caused  rather  by  warm  water  currents  than  by
the  change  of  environmental  conditions  (Figs. 2,  5).  Nev-
ertheless,  the  different  character  of  the  nannofossil  as-
semblages  in  the  western  and  eastern  fans  may  also
indicate  different  ecological  conditions.  Moreover,  dis-
coasters  appear  during  Zone  NN6,  Serravalian  in  the
western  fan,  but  in  the  eastern  fan  were  not  recorded.  Ac-
cording  to  Young  (1999)  discoasters  reflect  oligotrophic
environments.

According to the distribution of trace fossil content, the

inner  part  of  both  fans  represent  Skolithos-Cruziana  ichno-
facies  and  eutrophic  condition.  However,  the  middle  part  of
both  fans  have  mixed  ichnoassemblages  (Skolithos-Cruzi-
ana  ichnofacies  and  Nereites  ichnofacies)  that  show
eutrophic-oligotrophic  conditions  while  the  outer  fans  indi-
cate  Nereites  ichnofacies,  and  oligotrophic  conditions.  The
distributions  of  the  trace  fossil  assemblages  show  that  the
eastern  fan  has  more  mixed  assemblages  than  the  western  (in
the  middle  of  the  fan).  On  the  other  hand,  the  fan  fringe  envi-
ronment  has  Ophiomorpha  isp.  It  can  be  explained  by  the  im-
port  of  its  trace  marker  within  stronger  turbidity  currents  from
the  inner  part  of  a  deep-sea  fan,  or  by  normal  ‘planned’  colo-
nization  (Uchman  &  Demircan  1999a,b)  (Figs. 2,  5).

Fig. 7. Correlation schema of the standard nannoplankton zones
with results of this study.

Fig. 6. Correlation schema of the planktonic foraminiferal zones with results of this study.

DEMùRCAN and YILDIZ

Conclusions

The sediments of the western fan (Kalaycôlar section)

and  eastern  fan  (Ku çusofulu  section)  of  the  Cingöz  For-
mation,  southern  Turkey  contained  well  preserved  plank-
tonic  foraminifers  and  calcareouss  nannofossils.

The assemblages of planktonic foraminifers comprise 11

species  of  6  genera  and  are  correlated  with  the  Praeorbuli-
na  glomerosa  curva  and  Orbulina  suturalis  Zones.  The
calcareous  nannofossil  associations  are  composed  of  27
species  of  10  genera  and  give  evidence  for  the  standard
nannoplankton  Zones  NN5  Sphenolithus  heteromorphus
and  NN6  Discoaster  exilis.  According  to  the  biostrati-

graphic  data,  sediments  of  the  Cingöz  Formation  are  at-
tributed  to  the  Langhian  and  Serravalian  Stages  of  the
Middle  Miocene.

In the depositional area of the Cingöz Formation, the

distribution  and  percentage  abundances  of  temperature
sensitive  planktonic  foraminifers  and  calcareous  nanno-
fossils  indicate  temperate  to  cold  sea  waters  in  the  Lang-
hian—Serravalian  interval.  A  different  situation  is  found
in  the  Serravalian  sediments  of  the  western  fan  where  cal-
careous  nannofossils  give  evidence  for  the  rise  in  temper-
ature  caused  probably  by  warm  water  currents  and  the
occurrence  of  discoasters  reflects  oligotrophic  condi-
tions.

Fig. 8. a  – Ophiomorpha isp.,  endichnial full-relief in coarse—medium-grained sandstone, inner fan; b  – Thallassinoides isp.,  endich-
nial  full-relief  in  medium-grained  sandstone,  middle  fan;  c  –  Halopoa  annulata  (Uchman),  hypichnial  full-relief  in  fine-grained  sand-
stone,  levee  and  inter  channel;  d  –  Zoophycos  isp.,  and  Phycodes  isp.,  endichnial  semi-relief  in  medium—fine-grained  sandstone,  fan
fringe/middle  fan;  e  –  Zoophycos  isp.,  endichnial  semi-relief  in  medium—fine-grained  sandstone,  slope/middle  fan;  f  –  Echinospira
isp.,  endichnial  semi-relief  in  fine-grained  sandstone,  middle  fan;  g  –  Scolicia  vertebralis  Ksiazkiewicz,  epichnial  full-relief  in  fine-
grained  sandstone,  middle  fan;  h  –  Helminthorhaphe  flexuosa  Uchman,  hypichnial  semi-relief  in  fine-grained  sandstone,  outer  fan
lobes/fan fringe; i – Lophoctenium isp., hypichnial full-relief in fine-grained sandstone, outer fan.

BIOSTRATIGRAPHY OF THE MIOCENE SUBMARINE FAN (SOUTHERN TURKEY)

Fig. 9.  a  –  Phymatoderma  isp.,  hypichnial  full-relief  in  fine-grained  sandstone,  middle  fan/outer  fan;  b  –  Nereites  irregularis  (Schaf-
häutl),  endichnial/endichnial full-relief in fine-grained sandstone, outer fan lobes/fan fringe;  c  – Paleodictyon majus Meneghini and  Plano-
lites  isp.,  hypichnial  semi-relief  in  fine-grained  sandstone,  outer  fan  lobes/fan  fringe;  d  –  Paleodictyon  delicatum  Uchman,  hypichnial
semi-relief in fine-grained sandstone, outer fan lobes/fan fringe; e – Scolicia prisca De Quatrafages, endichnial semi-relief in fine-grained
sandstone, middle fan; f – Scolicia strozzii (Savi et Meneghini), hypichnial semi-relief in fine-grained sandstone, middle fan/outer fan;
g – Cosmorhaphe isp., hypichnial semi-relief in fine-grained sandstone, outer fan lobes/fan fringe; h – Cosmorhaphe sinuosa (Azpeita),
hypichnial semi-relief in fine-grained sandstone, outer fan lobes/fan fringe; i – Helminthorhaphe flexuosa Uchman, hypichnial semi-relief
in fine-grained sandstone, outer fan lobes/fan  fringe.

The Cingöz Formation consists of 24 ichnotaxa and the

inner  part  of  both  fans  representing  Skolithos-Cruziana  ich-
nofacies  and  eutrophic  conditions.  The  middle  part  of  both
fans  have  mixed  ichnoassemblages  (Skolithos-Cruziana
ichnofacies  and  Nereites  ichnofacies)  that  show  eutrophic-
oligotrophic  conditions.  Nereites  ichnofacies  and  olig-
otrophic  conditions  are  indicated  in  the  outer  part  of  the
eastern  fan.  According  to  these  data  the  upper  level  of  the
eastern  fan  characterized  a  deeper  environment  than  the
western  fan.  The  fan  fringe  environment  has  Ophiomorpha
isp.  It  can  be  explained  by  import  of  its  trace  marker  within
stronger  turbidity  currents  from  the  inner  part  of  the  deep-
sea  fan,  or  by  normal  ‘planned’  colonization.

Acknowledgments:  This  study  is  a  part  of  Phd.  Thesis  of
Huriye  Demircan.  First,  we  would  like  to  thank  Polish
Embassy  for  Providing  scholarship  to  us  for  staying  in
Poland.  Also,  authors  thank  to  Prof.  Dr.  Gilbert  Kelling
(Aberdeen  University)  for  selecting  this  study  area  and  fi-
nancial  support,  Prof.  Dr.  Kemal  Gürbüz  and  Prof.  Dr.  Ve-
dia  Töker  for  advising  us.

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DEMùRCAN and YILDIZ

Globigerina falconensis Blow, 1959
Globigerina  woodi  connecta  Jenkins,  1964
Globigerinoides  bisphericus  Todd,  1954
Globigerinoides  subquadratus  Brönnimann,  1951
Globigerinoides trilobus (Reuss, 1850) Grimsdale, 1951
Globoquadrina altispira conica Brönnimann et Resig, 1971

Appendix

List of planktonic foraminiferal species mentioned in this study

Globoquadrina dehiscens (Chapman, Par et Collins, 1934) Blow,

1959

Globorotalia peripheroronda Blow et Banner, 1966
Praeorbulina glomerosa curva Blow, 1956
Orbulina bilobata (d’Orbigny, 1846) Palmer, 1941
Orbulina suturalis Brönnimann, 1951

List of calcareous nannoplankton species mentioned in this study

Braarudosphaera bigelowii (Gran et Braarud, 1935) Deflandre,

1947

Coccolithus miopelagicus Bukry, 1971
Coccolithus pelagicus (Wallich, 1877) Schiller, 1930
Coronocyclus nitescens (Kamptner, 1963) Bramlette et Wilcoxon, 1967
Dictyococcites productus (Kamptner, 1963) Backman, 1980
Discoaster aulakos Gartner, 1967
Discoaster exilis Martini et Bramlette, 1963
Discoaster variabilis Martini et Bramlette, 1963
Helicosphaera burkei Black, 1971
Helicosphaera intermedia Martini, 1965
Helicosphaera kamptneri Hay et Mohler in Hay et al., 1967
Helicosphaera sellii Bukry et Bramlette, 1969
Helicosphaera orientalis Black, 1971

Helicosphaera  philippinensis  Müller,  1981
Helicosphaera walbersdorfensis Müller, 1974
Pontosphaera  inconspicua  (Sullivan,  1964)  Perch-Nielsen,  1984
Pontosphaera  japonica  (Takayama,  1967)  Nishida,  1971
Pontosphaera  multipora  Roth  (Kamptner,  1948)  Roth,  1970
Pontosphaera  scutellum  Kamptner,  1952
Reticulofenestra  haqii  Backman,  1978
Reticulofenestra minutula (Gartner, 1967) Haq et Berggren, 1978
Reticulofenestra  pseudoumbilica  (Gartner,  1967)  Gartner,  1969
Sphenolithus abies Deflandre in Deflandre et Fert, 1954
Sphenolithus capricornutus  Bukry et Percival, 1971
Sphenolithus  conicus  Bukry,  1971
Sphenolithus  heteromorphus  Deflandre,  1953
Triquetrorhabdulus rugosus Bramlette et Wilcoxon, 1967

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