GEOLOGICA CARPATHICA, APRIL 2005, 56, 2, 113122
Famennian conodonts from the Ayineburnu Formation of the
Istanbul Zone (NW Turkey)
ýENOL ÇAPKINOLU
Department of Geological Engineering, Karadeniz Technical University, TR-61080 Trabzon, Turkey;
capkin@risc01.ktu.edu.tr
(Manuscript received October 2, 2003; accepted in revised form June 16, 2004)
Abstract: Limestone samples from three incomplete stratigraphic sections of the Upper Devonian Ayineburnu Forma-
tion in the Denizliköyü area, Gebze, northwestern Turkey produced conodont faunas, which can be correlated with
established Famennian conodont zones. The sections (D, DN and DB) consist mainly of interbedded planar to nodular
limestones and dark shales, indicative of slope sedimentation. The sections D and DN define an interval extending from
the Lower marginifera Zone into the postera Zone, and fill the gap between the former studied sections of the Ayineburnu
Formation. The section DB contains the Lower and Middle expansa Zones.
Key words: Famennian, NW Turkey, Istanbul Zone, biostratigraphy, conodonts.
Introduction
The first conodont faunas from the Upper Devonian Ayine-
burnu Formation were reported by Abdüsselamoûlu (1963)
and Haas (1968a,b). Initial conodont biostratigraphic studies
and recognition of the established zonation scheme of Zie-
gler (1962, updated by Ziegler & Sandberg 1984, 1990) are
more recent (Çapkônoûlu 1997, 2000, 2005). In the outcrop
area in the Istanbul Zone of the Pontides (Fig. 1) no com-
plete section of the Ayineburnu Formation has been de-
scribed, therefore the conodont zones have been recognized
from different sections (Fig. 2). The Famennian Upper rhom-
boidea and Lower marginifera Zones are recognized in the
Büyükada (Istanbul) section (Çapkônoûlu 1997). The con-
odont faunas of the two incomplete sections sampled from
the Denizliköyü area are assigned to the Lower, Middle, and
Upper expansa Zones (Çapkônoûlu 2000). Conodonts of the
Upper rhenana Zone (Frasnian) to the Uppermost crepida
Zone (Famennian), excepting the Lower triangularis Zone,
have been found in the Tuzla section in the Tuzla Peninsula,
Istanbul (Çapkônoûlu 2005). Three new sections of the Ay-
ineburnu Formation, documented herein, span an unsampled
interval between the former sections that represent an inter-
val extending from the Lower marginifera Zone into the
Middle expansa Zone (Figs. 2 and 3).
Geologic setting and stratigraphy
General the Istanbul Zone of the Pontides (Fig. 1) com-
prises a thick OrdovicianEarly Carboniferous sedimentary
sequence, deposited on a passive margin, changing to an ac-
tive margin after the late Visean (Seymen 1995; Okay et al.
1996). This Paleozoic sequence, folded and possibly thrust-
faulted during the Late CarboniferousPermian Hercynian
Orogeny, lies unconformably over a Precambrian crystalline
basement, exposed in the Karadere area of Kastamonu (Arpat
et al. 1978), and is unconformably overlain by Triassic or
younger sedimentary rocks (Özdemir 1971; Gedik 1975).
The rocks of the Istanbul Zone show different tectonic and
stratigraphic characteristics in the areas to the east and west of
Kocaeli. On the basis of their different PaleozoicMesozoic
history, Kozur & Göncüoûlu (1998) suggested that the Istan-
bul Zone belongs to two different terranes: the Istanbul Ter-
rane consists of a PaleozoicMesozoic sequence around Istan-
bul-Gebze, and the Zonguldak Terrane of the Çamdaû,
Zonguldak, Amasra and Safranbolu regions. Similar Paleozoic
sequences are known only from the Balkan Peninsula and
Central Europe. The stratigraphic similarity between the Istan-
bul Zone and the Moesian Platform has been noted, and the
former is interpreted by some as a Hercynian fragment rifted
from the southern margin of Laurasia during the Late Creta-
ceous (Okay et al. 1994, 1996). Kalvoda et al. (2003) also not-
ed that there are close similarities between Neoproterozoic and
Paleozoic strata(?) in the Brunovistulian Terrane of central
Europe and the Istanbul Zone.
Ayineburnu Formation the Denizliköyü area, some
75 km southeast of Istanbul and 20 km northeast of the town
of Gebze, Kocaeli, is the major outcrop area of the Ayinebur-
nu Formation, which forms the Upper Devonian part of the
thick, Paleozoic sedimentary sequence of the Istanbul Zone
(Fig. 1). The Ayineburnu consists of dark grey, nodular- to
planar-bedded lime mudstones, interbedded with dark grey
shale to marl partings or beds, and locally contains some chert
nodules and interbeds. Sedimentological features indicate
deposition in a slope environment (Önalan 1982, 1988; Sey-
men 1995), supported by an offshore palmatolepid-polyg-
nathid conodont fauna (Çapkônoûlu 1997, 2000). Many sec-
tions are faulted and overturned or covered by soil as indicated
in previous papers (Çapkônoûlu 1997, 2000, 2005), and there-
fore accurate estimates of the thickness of the Ayineburnu
Formation are not possible.
www.geologicacarpathica.sk
114 ÇAPKINOLU
The name Ayineburnu Formation is used, in this study, as
equivalent of the Ayineburnu Member of previous papers
(Kaya 1973; Önalan 1982, 1988; Çapkônoûlu 1997, 2000,
2005). Furthermore, it is synonymous with nodular lime-
stones (Abdüsselamoûlu 1963), Denizli beds (Haas
1968a,b), and Denizli formation (Seymen 1995). The con-
tacts with the underlying Yörükali Formation (the former
Yörükali Member), and overlying Baltalimanô Formation are
conformable (Kaya 1973; Önalan 1982). More detailed works
related to the stratigraphy, sedimentology, and paleotectonic
setting have been undertaken (Kaya 1973; Önalan 1982, 1988;
Seymen 1995; Okay 1996).
Studied stratigraphic sections three sections (D, DN and
DB) of the Ayineburnu Formation in the Denizliköyü area
were measured (Figs. 1 and 3). All the sections are incom-
plete, and have generally faulted lower and upper contacts.
They are easily accessible on the north and west sides of
Deûirmenbayôrô Hill. Section D, about 67 meters thick, is lo-
cated on the north side of the Denizli highway and parallel to
the road. Section DN is about 36 meters thick and nearly nor-
mal to the road. Section DB, 31.50 m thick, is on the north
Fig. 1. Maps showing the tectonic units of Turkey (Okay et al. 1996), the location of the study area and the studied stratigraphic sections.
ISZ Istanbul Zone, SZ Sakarya Zone, BFZ Bornova Flysch Zone, NAFZ North Anatolian Fault Zone, EAFZ East Anatolian
Fault Zone, BSZ Bitlis Suture Zone.
side of Deûirmenbayôrô Hill. Strata consist of limestone and
interbedded shale or marl; sections D and DN are overturned.
Conodont biostratigraphy
Conodonts, abundant ostracodes, less trilobite and brachio-
pod shells, as well as rare fish teeth and scales were recovered
by formic acid-leaching of limestone samples from three mea-
sured sections (D, DN, and DB) of the Ayineburnu Formation
(Fig. 3). The materials consist of 93 samples, of which 45 pro-
duced the conodont faunas (Tables 13). Conodont yields
were sparse, averaging less than ten specimens per kilogram
of rock processed. Only eighteen samples yielded more than
ten conodonts per kilogram of rock. The fossiliferous samples
are poor in both diversity and population.
Section D section D represents an interval ranging from
the Lower marginifera Zone into the postera Zone (Fig. 3; Ta-
ble 1). The co-occurrence of Palmatolepis quadrantinodosa
inflexoidea and Palmatolepis marginifera marginifera in sam-
ple D22 defines the Lower marginifera Zone (see Ziegler &
FAMENNIAN CONODONTS OF THE ISTANBUL ZONE (NW TURKEY) 115
Fig. 2. The relative position and correlation of Upper Devonian stra-
ta in NW Turkey compared to stage boundaries and the conodont
zonation of Ziegler (1962) most recently revised by Ziegler & Sand-
berg (1990).
Sandberg 1984, Fig. 2). The lower strata are questionably as-
signed to this zone, due to the absence of taxa characteristic of
older zones. A badly broken specimen questionably referred
to Palmatolepis rugosa trachytera, the index taxon of the tra-
chytera Zone, was recovered in sample D8. Therefore, the
samples D20 to D9 can be correlated with the Upper and Up-
permost marginifera Zones. The overlying samples D8 and
D7 represent the trachytera Zone. Sample D6a contains
Polygnathus obliquicostatus, which first appears at the base of
the postera Zone (Ziegler & Sandberg 1984, Fig. 3), and
therefore it is within this zone. The overlying strata are as-
signed to the postera Zone due to the absence of defining taxa
of any younger zones.
Section DN section DN contains conodont faunas rang-
ing from the Lower marginifera Zone or probably the Upper
rhomboidea Zone into the postera Zone (Fig. 3; Table 2). The
name-bearer taxon, Palmatolepis marginifera marginifera,
was only found in samples DN14 and DN13 (Table 2). How-
ever, the lowest part of the section defines the Lower margin-
ifera Zone, based on the occurrence of Palmatolepis quadran-
tinodosa inflexoidea in sample DN18 and Palmatolepis
quadrantinodosa inflexa in sample DN14, both of which are
mainly restricted to this zone (Ziegler & Sandberg 1984,
Fig. 2), but it may extend into the older Upper rhomboidea
Zone. The overlying samples DN13DN9 do not contain zon-
ally diagnostic conodonts, but they can be correlated to the
Upper marginifera to trachytera Zones, on the basis of the
first occurrence of Polygnathus obliquicostatus in sample
DN7a. Due to the lowest occurrence of Polygnathus
obliquicostatus, sample DN7a is within the postera Zone.
Higher samples have also been assigned to this zone due to the
lack of any taxa typical of younger zones.
Section DB Conodont faunas of section DB are assigned
to the Lower and Middle expansa Zones (Fig. 3; Table 3).
Palmatolepis gracilis expansa, index species of the expansa
Zone, occurs only in sample DB3. Sample DB23 is in the
Fig. 3. Columnar sections of the studied sections of the Ayinebur-
nu Formation at the Denizliköyü area showing lithology, and units
sampled for conodonts.
116 ÇAPKINOLU
Table 2: Distribution of conodonts in the DN section of the Ayineburnu Formation in the Denizliköyü area, Gebze, Kocaeli, NW Turkey.
ZONE
U. rhomboidea? -
Lower marginifera
Upper marginifera-trachytera
postera
SAMPLE
DN18 DN15 DN14 DN13 DN12 DN11 DN10 DN9 DN7a DN7 DN5 DN4 DN3 DN2
SAMPLE WEIGHT (kg)
0.70 0.50 0.70 0.70 0.40 0.40 0.45 0.50 0.70 0.60 0.90 0.80 0.75 0.50
Palmatolepis minuta minuta
2
Palmatolepis perlobata schindewolfi
1
1
3
Palmatolepis quadrantinodosa inflexoidea
1
Palmatolepis rhomboidea
1
Palmatolepis glabra acuta
1?
Palmatolepis glabra lepta
1
Palmatolepis glabra pectinata
6
4
Palmatolepis glabra prima
8
1
Palmatolepis gracilis gracilis
12
1
2
1?
Palmatolepis marginifera marginifera
7
1
Palmatolepis quadrantinodosa inflexa
4
Polygnathus glaber glaber
1
Bispathodus stabilis
1
6
2
Branmehla gediki
1
2
6
Mehlina strigosa
3
2
4
1
3
Palmatolepis rugosa cf. ampla
2
Polygnathus diversus
1
Polygnathus communis communis
1
Polygnathus rhabdotus
2
Polygnathus obliquicostatus
1
1
Polygnathus styriacus
6
2
1
6
Branmehla inornata
2
1
1
Branmehla bohlenana
1
2
Palmatolepis rugosa ampla
4
Palmatolepis gracilis sigmoidalis
3
Polygnathus marginvolutus
4
Table 1: Distribution of conodonts in the D section of the Ayineburnu Formation in the Denizliköyü area, Gebze, Kocaeli, NW Turkey.
ZONE
Lower marginifera
Upper and Uppermost marginifera
trachytera post.
SAMPLE
D41 D39 D24 D22 D20 D18 D15 D14a D11 D10 D9
D8
D7 D6a
SAMPLE WEIGHT (kg)
0.60 0.50 1.35 1.00 1.00 1.10 0.70 0.45 0.70 0.90 1.00 0.55 0.70 0.50
Palmatolepis glabra pectinata
1
1
3
6
Mehlina strigosa
1
1
2
2
2
Palmatolepis glabra prima
1
1
2
4
Palmatolepis minuta minuta
1
3
2
1
2
Palmatolepis gracilis gracilis
1
3
Palmatolepis marginifera marginifera
1
1
1
4
Palmatolepis quadrantinodosa inflexoidea
1
Palmatolepis glabra lepta
1
1
Polygnathus glaber glaber
1
Palmatolepis glabra acuta
1
1
Polygnathus subnormalis
3
2
Palmatolepis glabra distorta
1
Palmatolepis gracilis sigmoidalis
1
Palmatolepis perlobata schindewolfi
1
1
4
1
Palmatolepis rugosa trachytera
1?
Polygnathus communis communis
1
Polygnathus obliquicostatus
1
Lower expansa Zone according to the occurrence of Polyg-
nathus styriacus, which is last known at the end of this zone
(Ziegler & Sandberg 1984, Fig. 2). Furthermore, the next
younger sample DB24 records the first occurrence of Bis-
pathodus aculeatus, which defines the base of the Middle ex-
pansa Zone. This indicates that the samples DB3DB23 be-
long to the Lower expansa Zone. The overlying samples are
assigned to the Middle expansa Zone due to the absence of di-
agnostic taxa of the younger zones.
Systematic paleontology
The familial classification proposed by Sweet (1988) is fol-
lowed here. Conodont faunas belong to the families Icriodon-
tidae (1 taxon), Palmatolepidae (19 taxa), Polygnathidae (11
taxa), and Spathognathodontidae (5 taxa), Unknown (3 taxa).
Because most of the forms encountered in the study have been
documented in previous papers, they are not formally de-
scribed but are recorded on the distribution tables (Tables 13)
FAMENNIAN CONODONTS OF THE ISTANBUL ZONE (NW TURKEY) 117
ZONE
Lower expansa
Middle expansa
SAMPLE
DB3 DB5 DB6 DB8 DB12 DB13 DB14 DB17 DB18 DB19 DB21 DB22 DB23 DB24 DB25 DB26 DB27
SAMPLE WEIGHT (kg)
1.15 0.90 0.70 1.00 0.60 0.80 1.00 0.50 0.85 1.00 1.15 0.80 0.85 1.00 0.65 0.70 0.80
Palmatolepis gracilis expansa
1
Palmatolepis gracilis gracilis
1
2
1
1
1
6
1
2
1
6
2
Palmatolepis gracilis sigmoidalis
3
1
5
1
3
7
3
4
2
1
Palmatolepis perlobata schindewolfi
2
2
3
3
1
2
1
4
4
Polygnathus perplexus
1
Polygnathus rhabdotus
2
1
6
Bispathodus stabilis Morphotype1
2
1
2
3
2
1
1
Mehlina strigosa
1
1
3
2
1
7
1
14
13
3
Polygnathus obliquicostatus
2
Icriodus alternatus alternatus
1
Polygnathus extralobatus
1
1
Polygnathus styriacus
1
5
3
5
1
1
4
6
8
Polygnathus granulosus
1
Branmehla gediki
12
13
5
2
3
7
1
Branmehla bohlenana
1
2
Branmehla inornata
7
3
2
14
4
Palmatolepis rugosa ampla
3
1
3
8
1
Palmatolepis gracilis manca
1
Polygnathus cf. irregularis
1
1
Polygnathus marginvolutus
2
Polygnathus communis communis
17
Pseudopolygnathus cf. dentilineatus
2
Bispathodus aculeatus plumulus
2
Bispathodus jugosus
6
Table 3: Distribution of conodonts in the DB section of the Ayineburnu Formation in the Denizliköyü area, Gebze, Kocaeli, NW Turkey.
and illustrated on plates (Figs. 45). All the samples are
housed in the Department of Geological Engineering, Kara-
deniz Technical University, Trabzon.
Family: Palmatolepidae Sweet, 1988
Genus: Palmatolepis Ulrich et Bassler, 1926
Type species: Palmatolepis perlobata Ulrich et Bassler, 1926
Palmatolepis rugosa cf. ampla Müller, 1956
Fig. 4.9
1960 Palmatolepis rugosa ampla Müller Ziegler in Kronberg et al.,
pl. 1, Figs. 34 (only)
1962 Palmatolepis rugosa ampla Müller Ziegler, pl. 8, Fig. 6 (only)
1967 Palmatolepis rugosa ampla Müller Wolska, pl. 11, Fig. 10
(only)
Remarks: The present Pa elements referred to this sub-
species closely resemble those of Palmatolepis rugosa ampla
but differ in the arrangement of nodes in the anterior part of
the outer platform. Palmatolepis rugosa ampla (Fig. 4.74.8)
bears a single row of large nodes in the anterior part of its out-
er platform, which forms a posterioward-directed acute angle
with the blade, whereas the older form Palmatolepis rugosa
cf. ampla has many random nodes in the same position.
Palmatolepis rugosa trachytera Ziegler, 1960
1960 Palmatolepis rugosa trachytera Ziegler in Kronberg et al., p. 38,
pl. 1, Fig. 6, pl. 2, Figs. 19
1984 Palmatolepis rugosa trachytera Ziegler Ziegler et Sandberg,
p. 187188, pl. 1, Figs. 15, 12 (see synonymy)
Remarks: One incomplete Pa element not illustrated
here has questionably been assigned to this taxon on the ba-
sis of the posterior part forming a nearly right angle with the
carina.
Family: Polygnathidae Bassler, 1925
Genus: Polygnathus Hinde, 1879
Type species: Polygnathus dubius Hinde, 1879
Polygnathus diversus Helms, 1959
Fig. 5.7
1959 Polygnathus diversa Helms, p. 650651, pl. 5, Figs. 58; text-
Fig. 2
1961 Polygnathus diversa Helms Helms, p. 681, pl. 1, Figs. 46;
pl. 2, Figs. 25; text-Fig. 2a,c
1966 Polygnathus diversa Helms Glenister et Klapper, p. 828,
pl. 94, Fig. 7
1967 Polygnathus diversa Helms Wolska, p. 412, pl. 16, Figs. 6, 7
1985 Polygnathus diversus Helms Olivieri, pl. 7, Figs. 25
1990 Polygnathus diversus Helms Perri et Spalletta, p. 6465, pl. 4,
Fig. 8a,b
Remarks: The free blade offset from the carina and the
platform ornament consisting of need-like denticles confined
mainly to the platform margins bordering the shallow adcari-
nal troughs are the most important features defining the Pa el-
ement of this species. The anterior outer margin commonly
extends farther anteriorly than the inner margin, giving the
platform an asymmetrical appearance. The inner margin termi-
nates posterior of the offset point of the blade, and the outer
margin anterior of that position. The free blade is slightly
118 ÇAPKINOLU
Fig. 4. Famennian conodonts from the Ayineburnu Formation of the Istanbul Zone, NW Turkey. All figures are upper views of Pa elements
unless otherwise stated. 1 Palmatolepis glabra acuta Helms, 1963; Sample D14a. 2 Palmatolepis glabra pectinata Ziegler, 1962; Sam-
ple D9. 34 Palmatolepis glabra prima Ziegler et Huddle, 1969; 3 Sample D15, 4 Sample D24. 56 Palmatolepis glabra lepta
Ziegler et Huddle, 1969; 5 Sample D8, 6 Sample DN12. 78 Palmatolepis rugosa ampla Müller, 1956; 7 Sample DB22, 8
Sample DN13. 9 Palmatolepis rugosa cf. ampla Müller, 1956; Sample DN3. 10 Palmatolepis minuta minuta Branson et Mehl, 1934a;
Sample D22. 1112 Palmatolepis gracilis gracilis Branson et Mehl, 1934a; 11 Sample DB5, 12 Sample DB23. 1314 Palmatol-
epis gracilis sigmoidalis Ziegler, 1962; 13 Oblique-lateral view, sample DN2, 14 Oblique-lateral view, sample DB27. 1518 Pal-
matolepis perlobata schindewolfi Müller, 1956; 15 Sample D8, 16 Sample D9, 17 Sample DB6, 18 Sample DB17. 19 Palma-
tolepis gracilis expansa Sandberg et Ziegler, 1979; DB3. 2022 Palmatolepis quadrantinodosa inflexa Müller, 1956; 20 Sample D22,
21 Sample DN14, 22 Sample DN14. 23 Palmatolepis gracilis manca Helms, 1963; Sample DB19. 24 Palmatolepis quadrantino-
dosa inflexoidea Ziegler, 1962; Sample DN18. 2527 Palmatolepis marginifera marginifera Helms, 1959; 25 Sample D9, 26 Sam-
ple DN14, 27 Sample DN14. 28 Palmatolepis rhomboidea Sannemann, 1955; Sample DN18. All scale bars = 0.1 mm.
FAMENNIAN CONODONTS OF THE ISTANBUL ZONE (NW TURKEY) 119
shorter than the platform. The basal cavity occurs just posteri-
or of the anterior tip of the platform.
Polygnathus extralobatus Schäfer, 1976
Fig. 5.1
1976 Polygnathus extralobatus Schäfer, p. 143144, pl. 1, Figs. 1617,
2326, text-Fig. 2
1979 Polygnathus extralobatus Schäfer Sandberg et Ziegler, p. 188,
pl. 5, Fig. 11 (see synonymy)
1991 Polygnathus extralobatus Schäfer Perri et Spalletta, p. 7071,
pl. 5, Figs. 46
Remarks: The inner platform of the Pa element bears ob-
lique transverse ridges, which form a posteriorward-directed
acute angle with the carina as in Polygnathus obliquicostatus,
but its broadly expanded posterior platform distinguishes this
species from the latter. In addition, the outer platform bears
curved transverse ridges, which are set vertically to the carina
posteriorly and diagonally to it anteriorly. Posterior platform
has transverse ridges crossing the entire platform. Anterior plat-
form is conspicuously constricted with a rostral development.
Polygnathus granulosus Branson et Mehl, 1934a
Fig. 5.14
1934a Polygnathus granulosa Branson et Mehl, p. 246, pl. 20, Figs. 21, 23
1973 Polygnathus granulosus Branson et Mehl Ziegler in Ziegler
(Ed.), p. 361362, Polygnathus pl. 3, Figs. 67 (see synonymy)
1990 Polygnathus granulosus Branson et Mehl Perri et Spalletta,
p. 65, pl. 5, Figs. 4a5b
Remarks: The Pa element represented by a single speci-
men in the collection has a lanceolate platform ornamented
with indistinct rows of nodes oblique to the carina with larger
nodes anteriorly. The anterior smooth part of the platform is
steeply deflected downward. The free blade is approximately
one-third of the unit length.
Polygnathus marginvolutus Gedik, 1969
Fig. 5.22
1969 Polygnathus marginvolutus Gedik, p. 237, pl. 5, Figs. 28
1974 Polygnathus marginvolutus Gedik Gedik, p. 20, pl. 5, Figs. 28
1991 Polygnathus marginvolutus Gedik Perri et Spalletta, p. 71, pl. 6,
Figs. 12 (see synonymy)
Remarks: Pa element possesses a triangular platform
with the troughs narrowing and shallowing posteriorly, and
widening and deepening anteriorly. Upturned platform mar-
gins bear nodes or short transverse ridges. The anterior two-
thirds of the platform is sharply deflected downward. The cari-
na is slightly curved. The free blade is about one-half to
one-third of the platform length. The basal pit set in the keel is
generally too small to recognize.
Polygnathus obliquicostatus Ziegler, 1962
Fig. 5.25.3
1962 Polygnathus obliquicostatus Ziegler, p. 9293, pl. 11, Figs. 812
1975 Polygnathus obliquicostatus Ziegler Ziegler in Ziegler (Ed.),
p. 311312, Polygnathus pl. 5, Fig. 5 (see synonymy)
Remarks: Pa elements assigned to Polygnathus obliqui-
costatus have a platform with the prominent rostrum, and with
transverse ridges oblique to the carina on the inner platform and
perpendicular to it on the outer side, characteristic of this spe-
cies. It is distinguished from Polygnathus extralobatus, with a
broadly expanded outer platform and a more curved carina, by
absence of the outer expansion; from Polygnathus semicostatus
by having transverse ridges oblique to the carina on the inner
platform and a prominent rostrum. Pa elements of Polygnathus
semicostatus possess transverse ridges perpendicular to the cari-
na on the inner platform, and a well-developed platform tongue.
Polygnathus rhabdotus Schäfer, 1976
Fig. 5.55.6
1961 Polygnathus n.sp. A. Helms, p. 697, pl. 4, Figs. 23, 28, 29
1976 Polygnathus rhabdotus Schäfer, p.146, pl. 1, Figs. 1822
Remarks: A short free blade with about one-third of the
platform length, and a platform ornament consisting of strong
transverse ridges anteriorly and changing to transversely
aligned nodes on posterior two-thirds define the Pa element of
Polygnathus rhabdotus. The platform ornament of the juvenile
specimens consists of nodes restricted to the platform margins.
Except for the upper platform ornament, Pa element is closely
similar to that of Polygnathus pennatulus, but the platform, in
the latter, has well-developed, unbroken transverse ridges.
Polygnathus cf. irregularis (Thomas, 1949)
Fig. 5.95.10
Description: Pa element has a rhomb-shaped platform
with the rostral ridges and troughs confined to the anterior half
of the platform. The upper surface is ornamented with rows of
nodes diagonal to the carina anteriorly, and random nodes to
irregular rows of nodes posteriorly. The platform is asymmet-
rical and the widest in the midlength. The right side is broadly
expanded with nearly triangular outline, and the left side a
convex curve. The carina is straight to deflected laterally at
midlength, and may or may not extend to the posterior tip. The
short free blade is about one-fifth of the unit length.
Remarks: Pa element resembles those of Polygnathus ir-
regularis and Polygnathus subirregularis, but differs by its
widely expanded platform with a lobe-like development on
the right side. One of the illustrated samples (Fig. 5.10) has a
carina development with lateral deflection at midlength that is
similar to Polygnathus subirregularis, but Pa element of the
latter has a narrower and more elongate platform.
Family: Spathognathodontidae Hass, 1959
Genus: Bispathodus Müller, 1962
Type species: Spathodus spinulicostatus Branson, 1934
Bispathodus aculeatus plumulus
(Rhodes, Austin et Druce, 1969)
Fig. 5.16
1975 Bispathodus aculeatus plumulus (Rhodes, Austin et Druce,
1969) Ziegler in Ziegler (Ed.), p. 2930, Bispathodus
pl. 1, Figs. 810 (see synonymy)
120 ÇAPKINOLU
Fig. 5. Famennian conodonts from the Ayineburnu Formation of the Istanbul Zone, NW Turkey. All figures are upper views of Pa elements
unless otherwise stated. 1 Polygnathus extralobatus Schäfer, 1976; Sample DB23. 23 Polygnathus obliquicostatus Ziegler, 1962;
2 Sample DN7, 3 Sample DN5. 4 Polygnathus communis communis Branson et Mehl, 1934b; DB24. 56 Polygnathus rhabdotus
Schäfer, 1976; 5 Sample DB3, 6 Sample DN9. 7 Polygnathus diversus Helms, 1959; Sample DN12. 8 Polygnathus perplexus
Thomas, 1949; Sample DB3. 910 Polygnathus cf. irregularis (Thomas, 1949); 9 Sample DB23, 44, 10 Sample DB22. 1113
Polygnathus styriacus Ziegler, 1957; 11 Sample DN5, 12 Sample DB21, 13 Sample DB6. 14 Polygnathus granulosus Branson et
Mehl, 1934a; 14 Sample DB8. 15 Bispathodus jugosus (Branson et Mehl, 1934a); Sample DB24. 16 Bispathodus aculeatus plumu-
lus (Rhodes, Austin et Druce, 1969); Lateral view, sample DB24. 1718 Bispathodus stabilis (Branson et Mehl, 1934a); 17 Sample
DB21, 18 Sample DN4. 19 Icriodus alternatus alternatus Branson et Mehl, 1934a; Sample DB5. 2021 Pseudopolygnathus cf. den-
tilineatus Branson, 1934; 20 Sample DB24, 21 Sample DB4. 22 Polygnathus marginvolutus Gedik, 1969; Sample DN2. 23
Polygnathus glaber glaber Ulrich et Bassler, 1926; Sample DN14. 24 Polygnathus subnormalis Vorontzova et Kuzmin, 1984; Sample
D15. 2526 Branmehla gediki Çapkônoûlu, 2000; 25 Lateral view, sample DB21, 26 Inner-lateral view, sample DN14. 27 Bran-
mehla bohlenana (Helms, 1959); Lateral view, Sample D21. 2829 Mehlina strigosa (Branson et Mehl, 1934a); 28 Lateral view, Sam-
ple DB24, 29 Lateral view, Sample DN3. 3032 Branmehla inornata (Branson et Mehl, 1934a); 30 Lateral view, Sample DN5,
31 Lateral view, Sample DB24, 32 Lateral view, Sample DN5. All scale bars = 0.1 mm.
FAMENNIAN CONODONTS OF THE ISTANBUL ZONE (NW TURKEY) 121
Remarks: The present Pa elements possess a plume-like
anterior blade with reclined (recurved) denticles increasing the
heights posteriorly, the distinctive characteristic of Bispatho-
dus aculeatus plumulus. Three to four discrete denticles occur
on the right side of the blade.
Bispathodus jugosus (Branson et Mehl, 1934a)
Fig. 5.15
1934a Spathodus jugosus Branson et Mehl, p. 190-191, pl. 17, Figs.
19, 22(?)
1974 Bispathodus jugosus (Branson et Mehl) Ziegler, Sandberg et
Austin, p. 103, pl. 1, Figs. 3, 4; pl. 3, Figs. 19, 23, 26
Remarks: The Pa elements have a trough or a few germ
denticles inserted between the main and lateral row denticles
at the posterior tip of the blade, characteristic of this species.
Family: Unknown Sweet, 1988
Genus: Branmehla Hass, 1959
Type species: Spathodus inornatus Branson et Mehl, 1934a
Branmehla gediki Çapkônoûlu, 2000
Fig. 5.255.26
1991 Branmehla bohlenana Helms Perri et Spalletta, p. 58, 60, pl. 3,
Fig. 1a,c
1998 Branmehla bohlenana Helms Perri et Spalletta, p. 164165,
pl. 1.4.1, Fig. 4a,c
2000 Branmehla gediki Çapkônoûlu, p. 101, pl. 4, Figs. 16
Remarks: Distinctive characteristics of the Pa element of
Branmehla gediki are the short and low posterior process with
markedly smaller denticles than the anterior process, and the
subcircular basal cavity beneath the cusp. The basal cavity ex-
tends anteriorly and posteriorly as a slit-like groove.
Although the Pa element shows a close similarity to that of
both Branmehla werneri and Branmehla bohlenana they are
distinguished in the shape of the basal cavity and in the char-
acteristics of the posterior process (see Çapkônoûlu 2000).
Branmehla werneri has a narrow and elongate basal cavity be-
neath a low, wide cusp and greatly reduced posterior process,
and Branmehla bohlenana, has an elliptical basal cavity, the
long axis of which lies obliquely to the axis of the blade. The
Pa elements of Branmehla bohlenana commonly have a pos-
terior process with a gradually decreasing height posterior-
ward of the cusp and therefore, a convex upper profile. In the
Pa element of Branmehla gediki, the posterior process abrupt-
ly decreases to about half-height of the anterior process just af-
ter the cusp, and has an even upper profile. Furthermore it has
a more prominent cusp than Branmehla bohlenana.
Branmehla gediki was initially described from the expansa
Zone (Çapkônoûlu 2000), but occurs from the Lower margin-
ifera Zone into the Middle expansa Zone. Some specimens,
which have been referred to Branmehla bohlenana, have been
illustrated from the Lower expansa and Upper postera Zones
of the Carnic Alps, Italy (Perri & Spalletta 1991, 1998).
Conclusions
Upper Devonian conodont zones extending from the Lower
rhenana Zone to the Upper expansa Zone, except for the Low-
er triangularis and Lower rhomboidea Zones, have been rec-
ognized from the outcrop sections in different areas of the Up-
per Devonian Ayineburnu Formation in the Istanbul Zone,
NW Turkey (Fig. 2). The Tuzla section, measured in strata ex-
posed on the Tuzla Peninsula, contains the Frasnian-Famenni-
an (F/F) boundary (Çapkônoûlu 2005). The Lower triangularis
Zone, the base of which corresponds to the F/F boundary, is
poorly defined or absent in the Tuzla section, which is now
covered. The Lower rhomboidea Zone and the Lower through
Upper praesulcata Zones, the youngest conodont zones of the
Upper Devonian, the upper boundary of which corresponds to
the Devonian-Carboniferous (D/C) boundary, are also unrec-
ognized due to the sampling scheme. The D/C boundary is
probably in bedded cherts and siliceous shales bearing phos-
phatic nodules of the Baltalimanô Formation overlying the Ay-
ineburnu Formation in the Denizliköyü area. The sections
studied here span an interval extending from the Lower mar-
ginifera Zone into the Middle expansa Zone, and document
the unsampled interval between sections studied earlier
(Fig. 2).
Additionally, the range of Branmehla gediki, previously
known from the Lower and Middle expansa Zones (Çap-
kônoûlu 2000), is extended from the Middle expansa Zone
downward into the Lower marginifera Zone.
Acknowledgments: This research was partly supported by
Karadeniz Technical University (Trabzon, Turkey), Science
Foundation (Project No: 21.112.005.6). I would like to thank
D. Jeffrey Over of SUNY Geneseo, for critically reviewing the
manuscript, and ùsmet Gedik of KTÜ Department of Geologi-
cal Engineering, for his criticism and advice. I also thank M.C.
Perri, C. Girard and J. Hladil for reviewing the submitted
manuscript and making valuable suggestions.
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