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Geology of a new Late Miocene mammal locality in central Anatolia, Turkey
0 1999 Academic
des sciences
/ pditions
Palaeontology / PalPontologie (Vertebrate Palaeontology / Pa/&nto/ogie
scientifiques
et mbdicales
Elsevier
SAS. Tous droits
r&sew%
des VertPbr&
Geology of a new Late Miocene in central Anatolia, Turkey
mammal
locality
Gologie d’un nouveau gisement de mammij&es d’dge Mioc&e supkieur en Ana tolie ten trale, Turqu ie Nizamettin Kazancia, Sevket Senb*, Giirol Seyitoglu”, Hakan Araza, Baki VaroY, Levent Karadenizli” a Ankara Universitesi, Fen Fakiiltesi, Jeoloji h Laboratoire de palContologie du Museum c Laboratoire
de palPontologie
des vert&br&
d Laboratoire
de palkontologie
des vertbbr&,
(Received
Abstract
13 April
-
The
1999,
new
accepted
mammal
Miihendisligi BBliimO, 06100 national d’histoire naturelle, et paleontologie Esa 7073
12 July
locality
Louis de Bonisc,
humaine,
du CNRS,
Ankara, Turkey UMR CNRS 8569, universite
universitk
GeneviPve
8, rue Buffon,
de Poitiers,
86022
Pierre-et-Marie-Curie,
Bouvraind,
75005
Poitiers 75252
Paris,
cedex,
Paris cedex
France
France 05, France
1999)
of Akkasdagi
yielded
a rich
fauna
dated
as Middle
Turolian. It is situated in the southern part of the Cankiri-Corum Basin in central Anatolia. In the Akkasdagi area, the sedimentary deposits, mapped as the Kizilirmak Formation, consist of tuffs and lacustrine limestones intercalated with elastic deposits, whilst in its type section, situated deposits. Miocene,
to the north near Kizilirmak town, this formation is mainly formed of fluviatile Facies distribution and geological observations led to conclude that during the depositional centers migrated from the north to the south of this basin.
(0
1999
Acadkmie
Mammal
locality
des sciences
/ Late Miocene
/ iditions
scientifiques
/ stratigraphy
et medicales
/ correlation
Elsevier
SAS.)
/ Anatolia
Ri%umk - Le nouveau gisement de mammif~rcs i Akkasdagi, au sud du bassin de cankirixorum (Anatolie centrale), a livrii une abondante faune dati-e du Turolien moyen. Dans le secteur d’Akkasdagi, la s&ie sedimentaire attribuee a la formation de Kizilirmak comporte une succession de tufs et de calcaires lacustres, intercal& dans les sediments dhitiques. Cette succession diffhe de celle de la coupe type, situ& plus au nerd, qui est domint% par des d6p6ts fluviatiles. Les observations g6ologiques montrent qu’au tours du Mioche, le centre de s6dimentation a migri- du nord vers le sud. (0 1999 AcadPmie des sciences / fiditions scienlifiques et medicales Elsevier SAS.) gisement
de MammiEres
/ Miocene
suph-ieur
/ stratigraphie
/ corriAation
/ Anatolie
Version abregee (voir p. 508) 1. Introduction parts The principal aim of this paper is to present a newly discovered Late Miocene mammal locality (Akkasdagi) and its geological context. This work is part of an integrated geological study of Neogene deposits in the Cankiri-Corum Basin. Neogene deposits cover the major Note
pr&entCe
* Correspondence
par Philippe and
reprints.
de la terre
et des plan&es
/ f&h
Anatolian
ing the Late Cenozoic they record all tectonic
Taquet.
Sci. Paris, Sciences 1999.329,503-510
C. R. Acad.
of the
peninsula.
central and western Anatolia, and southern Anatolia. The times larger than the marine,
& Planefory
Sciences
They
are
terrestrial
in
but mainly marine in eastern terrestrial cover, which is 4-5 is of great interest for study-
tectonic phases
evolution and events.
of Turkey, A good
since under-
N. Kazanci et al. standing of their chronology is essential to interpret tectonic events and to construct basin evolution models. In central Anatolia, Early Miocene deposits are mainly lacustrine while the Middle-Late Miocene ones are mainly palustrine and fluviatile (LOttig and Steffens, 1976). The stratigraphy of these continental deposits is not yet well established, mainly because of (1) the presence of many small sedimentary basins with unclear borders, and (2) the frequent lateral facies changes in their deposits. Palaeontological research in these deposits are not extensive enough to build a detailed biostratigraphy of terrestrial deposits and to provide correlation between the lithologic units. The available stratigraphy of the central Anatolian basins is based at present on the geometric relationshipsof lithological unitsand on a few mammalian faunas. In the Cankiri-Corum Basin, a dozen mammal localities are already known (Sen et al., 1998), but they are situated in its northern and central parts, while the Akkasdagi locality is near the southern edge of this basin. As stressed in this paper, the present data are far from establishing a detailed stratigraphy of Neogene deposits. Consequently, all newly discovered mammal localities contribute to refining the current stratigraphic chart. The Akkasdagi mammal locality is situated in the southern part of the Cankirixorum Basin, NNW of Kaman town and some 3.5 km from GGkesme village (figure 7). Bones are concentrated on a thick tuff layer along the southwestern slopes of the hill, Akkasdagi.
2. Tectonic
setting and stratigraphy
The closure of the northern branch of Neotethys during the Late Cretaceous-Late Eocene created a complex tectonic pattern (Sengcir and Yilmaz, 1981; Seng6r and Natal’in, 1998). The closure occurred between irregular margins, therefore the evolutionary history of basins, including Cankiri-Corum Basin, is not correlative from one area to another (G&iir et al., 1984; Cater et al., 1991; Tiiystiz and Dellaloglu, 1992; Erdogan et al., 1996). Even within the Cankiri-Corum Basin, tectonic phases and structures in different subbasins show great differences (figure 7). Such a complex evolution led geologists to contradictory interpretations (Koc;yigit, 1991; TOysLiz and Dellaloglu, 1992; Erdogan et al., 1996; Seyitoglu et al., 1997). The progressive uplift of the Anatolian peninsula during the Miocene generated its continentalization, thus forming an intramontane plateau in central Anatolia. The origin of the present-day morphological features of the Anatolian plateau should thus be regarded as undergoing its tectonic evolution during the Neogene period (G&Or et al., 1995). The depression areas grouped under the name of Inner Anatolian Basins are in fact composed of the Cankiri-Corum, Tuzgiilti, Haymana and Sivas basins (figure I) which are the subsidence areas between the uplifted continental blocks (Birgili et al.,1 975; G&Or et al., 1984; Cater et al., 1991).
504
The Cankiri-corum Basin is filled with deposits ranging in age from Late Paleocene to Pleistocene. Three main periods of sedimentation are separated by two major angular unconformities: Late Paleocene-Late Eocene marine deposits, Early-Late Miocene fluviolacustrine (partly evaporitic) deposits, and Late Miocene-Pleistocene fluviatile deposits (Birgili et al., 1975). The earliest marine deposits crop out in the central and northern parts of the basin, while the later deposits are mainly exposed in the central and southern regions. This distributional pattern might be indicative of a southern shift of depositional centers. The uppermost continental deposits are formed under the control of active neotectonics that are encountered almost everywhere in the Anatolian plateau. Since the Pliocene, this basin has been bordered to the north by the North Anatolian transform fault (figure I). The contribution of volcanic products in the filling of the Cankiri-Corum Basin is known to have existed since the Eocene, with a maximum during the Late MiocenePliocene interval. The relationships of the tectonic dynamics in Cankiri-Corum Basin with the volcanic activity are unknown. However, this basin is surrounded, and even partly covered in the north, by two vast volcanic complexes, the Galatia and Cappadochia volcanic complexes. These volcanic complexes are in turn one of the main source areas for sediments infilling the Cankiri-Gorum Basin. The mammal-bearing tuff horizon at Akkasdagi and its surrounding areas probably originated from the northwestern edge of the Cappadocian volcanic complex. In summary, the Cankiri-Corum Basin developed during Late Paleocene to Oligocene under the postcollisional compressive tectonic regime (Tiiysiiz and Dellaloglu, 1992; Erdogan et al., 1996), which divided the basin into smaller subbasins in the Middle Eocene-Oligocene (Karadenizli et al., 1998). However, the tectonic style of Miocene-Quaternary evolution of the basin is a subject of current debate (Kocyigit et al., 1995; Seyitoglu et al., 1997).
3. Lithology sequence
of the fossiliferous
In the southern part of Cankiri-Corum Basin, Late Miocene deposits cover the metamorphic basement (Kirsehir Massif; Seymen, 1982), the granites which cut this massif, or the marine Eocene deposits. In the Akkasdagi area, Neogene deposits unconformably overlie the basement formed of granites, ophiolites and metamorphic rocks. The absence of older sedimentary rocks in the Cankiri-Corum Basin implies that the sedimentary units in the Akkasdagi area are an overlap following the southwestern development of this basin. The sedimentary deposits of the Akkasdagi area are mapped as Kizilirmak Formation dated as Late Miocene (Birgili et al., 1975; Seymen, 1982). However, Erdogan et al. (1996) proposed, by lithological correlation with similar deposits of the Cankiri-Gorum Basin, a Middle Miocene age, and considered them as ‘cover deposits’.
C. R. Acad. Sci. Paris, Sciences
de la terre
et des plan&es
/ Eatih
& Planetary Sciences 1999.329,503-510
A new
Figure 1. Simplified geoiogical map of north 2. Pontid block. 3. Sakarya block. 4. Calatia Carte geologique simplifiee 1. Bassins neogenes. 2. Bloc 7. ChaFne de Taurus.
de I’Anatolie de Pontides.
Sciences
de
nord-centrale et localisation 3. Bloc de Sakarya. 4. Complexe
la terre
Miocene
mammal
locality
from
central Anatolia with the main tectonostratigraphic units and Neogene basins. volcanic complex. 5. Ophiolitic formations. 6. Kirsehir Massif. 7. Taurus belt. des principales volcanique
The Akkasdagi fossiliferous horizon is a part of a Messa type hill which is about 2.5 km long in the NE-SW direction, and 1 km wide. Akkasdagi forms the major relief of the area and is highly visible because of its relief and light colour of sediments in contrast to the surrounding red, steppe landscape. The top of the hill is at 1 019 m altitude. The nearest village, Cokesme, is situated about 3 km southeast of the hill. The bone-bearing sites are along its soutwestern slopes at an altitude of 950 m (coordinates X = 4372500, Y = 0556000). figure 2 presents the typical lithological succession of the Akkasdagi deposits. Three noticable volcanoclastic horizons are intercalated in marls and clayey limestones capped by coarse elastic sediments. Conglomeratic lenses are quite frequent in levels above the fossiliferous tuffs, C. R. Acad. Sci. Paris, 1999 329,503~510
Late
et des
pIaWes
/ Earth
unites de Calatie.
tectonostratigraphiques 5. Formations ophiolitiques.
et des
central
Anatolia
1. Neogene
bassins 6. Massifde
basins.
neogenes. Kirsehir.
and lateral facies changes between clayey, marly, sandy and conglomeratic layers are also observed. These are interpreted as alluvial fans. The carbonate-rich clays of the lower part display a reddish colour because of oxidation. They also show nodular structures and frequent rootmarks in some horizons, probably indicative of shallow lacustrine depositional environments. The two lower volcanoclastic horizons are composed of fine-grained tuffs, while the third one is a coarse tuftit. The tuffs include gas segregation pipes which imply hot setting of the material (Gas and Wright, 1987). They do not show any clear lithification or graded bedding. Their thickness varies from 3 to 7 m (figure2). Their thickness and morphology indicate that they were settled as nyroclastic flow & hnetary
Sciences
N. Kozanci
et al
ulty of Sciences, studied the stratigraphy of the area and unearthed a reliable collection of mammals from Akkasdagi. in September 1997, the authors of this paper excavated three spots (labelled as AKA, AKB and AKK) along the same horizon to collect mammalian remains and taphonomic observations. We must stress that this mammal locality may disappear, or at least be severely damaged, if the project of an industrial company for exploitation of this tuff for cement row material is realized. The mammalian fauna presented below is based on the material collected between 1995 and 1997. Bones are accumulated in holes that are apparently dug out by erosion of the tuff surface; they are at most 1 m deep and 2 m wide. The matrix of fossilifereous pockets is also the tuff mixed with some elastic elements. The three bone pockets excavated in 1997 contain both large and small mammals. Among the large mammals, the perissodactyls and especially hipparions are predominant. They are represented by many skeletal remains often in connection, limb and cranial bones. The main part of specimens is not yet prepared; it is therefore not possible to determine them at the species level. Nevertheless, it seems that two species, perhaps three, are differentiated by size. Thus, the length of the third metatarsal varies from 236 to 285 mm and that of the third metacarpal from 185 to 240 mm. A rhinoceros is represented by some limb bones in all three bone pockets. The artiodactyls, although numerically less than the perissodactyls, are more varied since they include bovids, giraffids and suids. There are four bovid genera. The most abundant is a gazelle whose remains (cranium, horn cores, jaws) have been recorded from the three fossiliferous spots. It is a middle-sized species with short and robust horn cores (length between 8 and 12 cm), and with deep grooves especially on their posterior face. The premolars are rather short compared to the molars. The horn cores of this gazelle differ from that of Gaze/la pilgrimifrom Samos (Greece) in being shorter and strongly curved, from Gaze//a capricornis from Pikermi (Greece) by their mediolateral compression, and from Gaze/la deperdita from Mont Luberon (France) and Dytiko (Greece) in being less curved backward. This species is quite similar to that of Kemiklitepe A + B (Turkey; Bouvrain 1994). A juvenile skull fragment (from the pocket AKK) and four upper jaws (AKB) belong to the genus Protoryx. Beyond the generic characters of Protoryx (straight horn cores, large sinus extending into the pedicel, short premolars, molars with strong and pinched styles) the most striking feature of Protoryx from Akkasdagi is the strong hypsodonty (hypsodonty index of M3 - between 118-l 25) exceeding for example that of Protoryx from Maragha (Iran). Inversely, Protoryx from Kinik (Turkey; Kijhler, 1987) and from the upper levels of Kemiklitepe are quite comparable to the Akkasdagi specimens. The tribe Boselaphini, usually abundant in Eurasian Late Miocene localities, is very rare in Turkey, An upper jaw from AKB can be referred to a Tragoportax similar in size to T rugosifrons from Samos with however rather long
m 70
red Clastics
white clayey Limestones
brownish 30
grey Tuffites
grey Marls grey Tuffs
10
-MAMMALIAN FAUNA plnkish white Tuffs unconformity
Pre Neogene Figure 1 ithologie kasdagi.
2. Lithology des
of late
sediments
Miocene
deposits
du Miocene
sup&rieur
basement at Akkasdagi dans
section.
la coupe
d’Ak-
(Cas and Wright, 1987). The tuffits of the third volcanoelastic level are quite weathered. The source area of tuffs, and tufits is not yet known. There are two close andesitic outcrops to the northeast and southeast of Akkasdagi. Moreover, trachyte and rhyolite outcrops are located west of Kaman. Even though rnore detailed studies are needed to locate the source area, we hypothesize that these tuffs originated from these volcanics which belong to northwestern edge of Cappadocidn volcanic complex.
4. Mammal
fauna
This mammal locality was indicated to one of us (N.K.) by a villager. Later on our investigations revealed that it was already known, but not explored, by palaeontologists. In his PhD thesis Ozansoy (1958) notes that “Dr. Burchart recently discovered a fauna with Hipparion gracile at Kaman”. Ayan (1963), when studying the petrography of different formations in the Kaman area, rediscovered this locality, and he illustrated some specimens as Hipparion grab/e. The locality was visited by E. Heintz on 21 October 1971; he collected 229 specimens, preserved in the Natural History Museum of Paris. During the 1995-l 996 field seasons, geologists from the Ankara University, Fac-
506
C
R. Acad
Sci
Paris,
Sciences
de
la terre
et des
plan&es
/ Earth
& Planetary Sciences 1999.329.503-5 10
A new
premolars. Tragoportax has not been found at Kemiklitepe, but it was mentioned at Kinik (K6hler, 1987). An antelope with spiral horn cores, assigned to Prostrepsiceros, is represented by a frontlet (AKK) and a partial horn core (AKB). It resembles frostrepsiceros rotundicornis from Pikermi in not having a transverse compression on the horn core, but it differs in having a deep anteromedial groove. Such a groove is known on horn cores of F! libycus from Sahabi (Libya) that is however a little larger in size (Lehmann and Thomas, 1987). The genus Prosfrepsiceros is rare in Turkey; nevertheless Senyiirek (1952) illustrated two horn cores from GBkdere. This genus is absent both at Kinik and Kemiklitepe. Giraffid remains are rare, only some limb bones were found in the three bone pockets. According to their size they could belong to a Samotherium, quite similar to that of Kemiklitepe A+B (Geraads 1994). However a phalanx and a fragment of calcaneum from AKK are clearly smaller and could be assigned to a Palaeotragus. Suids are relatively abundant and represent the genus Microstonyx, which is the most widespread form both in Europe and central Asia during the Late Miocene. The lack of pl as well as the small size of the lower canine allow it to be determined as M. major. We must also mention the presence of a few proboscidian remains determined as Choerolophodon sp. The carnivora are present with two species of hyaenids. One of them, Hyaenothedum wongi, is represented by several specimens of isolated teeth and fragments of mandibles belonging to three different individuals. The size and proportions of teeth are similar to those of the specimens recovered from the Kemiklitepe locality in western Turkey (de Bonis, 1994). A large isolated lower premolar looks like those of small individuals of Adcrocuta eximia. It can be identified as A. cf. eximia. Aardvark remains were found in the spot AKK with a left manus and a right pes. In size, this animal is similar to Orycteropus gaudryi Major, 1888 from Samos (Mclll length = 46.5, Mtlll length = 69.2). Aardvarks are quite common in Middle-Late Miocene localities in Turkey and Greece (Colbert, 1941; Sen, 1994). This locality has also yielded small mammals in all three spots excavated. Some remains were collected during the 1997 excavations, while some others were obtained by sorting the residue after wet screening. We have to note that the tuff is hard to break up in water and to concentrate. A mandible and some isolated lower teeth belonging to an erinaceid insectivore were determined as Schizogalerix atticus (Rtimke, 1976). On ml and m2, the trigonid valley is narrow and deep, the posterior arm of the hypoconid is connected to the entoconid but not to the posterolophid. These characters are typical for S. attica from Chomateri (Greece), and the size of the Akkasdagi specimens also fits with this species. It seems that this genus has, in the Aegean area, an anagenetic evolution since only one lineage is recognized from the Early Astaracian (Pasalar, S. pasalarensis Engesser, 1980) to Latest Turolian (Amasya, Shizogalerix n. sp. , in Engesser, 1980). C. R. Acad Sci. Paris, Sciences 1999.329.503-510
de la terre
et des plan&es
/ farfh
Late Miocene
mammal
locality
from
central
Anatoiia
Among rodents, the family Cricetidae is present with two species of Byzantinia well distinguished in size and morphology. The largest form (Ml = 3.75 x 2.70 mm) is quite similar to B. hellenicus (Freudenthal, 1970) from Samos in having Ml widened, with a strong anterolabial spur and well developed ectolophs. The second form is smaller, Ml (3.45 x 2.25) without spur and with lower ectolophs. This second species is smaller than the previous one but larger than any other species of Byzantinia from the Late Miocene of Turkey and Greece (Bruijn, 1976; Unay, 1980). It is for instance determined as Byzantinia sp, The genus Byzantinia has been known in Turkey and Greece since the late Astaracian and it disappears towards the end of the Turolian. The paucity of the knowledge on its Late Miocene, mainly Turolian representatives means that its discovery in Akkasdagi is of great interest. Only one ml (I .88 x 1.22) of Muridae has been found at the spot AKK. Its dimensions, the presence of a small anteromedian cuspid and a wide posterior edge allow its comparison with Occitanomys provocator Bruijn, 1976 from Chomateri and Samos 53 (Greece, MN1 2). A worn M3 (2.04 x 2.42) and a damaged Ml (1.97 x 2.59) can only be determined as Spalacidae indet. and Sciuridae indet., respectively. Concerning the large mammals, the composition of the Akkasdagi fauna is similar to that of the upper level of Kemiklitepe or that of Kinik (figure 3), and indicates therefore a Middle Turolian age (MNI2). Among the small mammals, the characteristic taxa (Schizogalerix, Byzantinia and Occitanomys) are all previously known from the Middle Turolian localities in Greece (Chomateri and Samos S3). Some K/Ar and Ar/Ar ages are also available for the locality Samos S3 which is bracketed between two tuff horizons dated as 7.28 + 0.01 and 7.09 + 0.01 Ma respeclively (Swisher, 1996). These similarities are strong enough to date the Akkasdagi fossiliferous horizon as MN1 2.
5. Conclusions Kizilirmak Formation is the most extensive Late Miocene unit of Cankiri-Corum Basin. In its type locality, it is composed of red coloured and dominantly coarse elastics which are covered by gypsum deposits. The Akkasdagi area is also mapped as Kizilirmak formation (Birgili et al., 1975; Seymen, 1982) though the sedimentary unit in the study site is rather different from the type locality since it includes a carbonate-dominated palustrine sequence with volcanoclastic layers. A red elastic sequence similar to the type location of Kizilirmak Formation is observed on the uppermost levels of the Akkasdagi section (figure 2). Such a lithofacies distribution may indicate that the southern part of the basin was a relatively lower area with swamps and/or shallow lakes, while fluviatile environments predominated in the northern parts during the Late Miocene. Later, swamps and lakes moved toward the north, and the Akkasdagi area became purely terrestrial. Similar changes & Planetary
Sciences
507
N. Kazanci
et al
rrrrrr r ,*R?‘“r+rpL+
Figure +:>>.
3. Comparison
of the fauna1 composition
Comparaison diagrammes.
de la composition
or migrations
of depositional
whole central al., 1995).
Anatolia
The Akkasdagi of open woodland
resemblances
with
the
those
des gisements
environments
that
were
(A) with
d’Akkasdagi
typical
in
(G&Or
et
assemblage is characteristic were dominant during
the
throughout
mammalian habitats
Turolian in southeastern The composition of
faunique
of Akkasdagi
the
Europe and Akkasdagi of other
Acknowledgements. The Akkasdagi was done with the support of Ankara Karakus. TUBITAK and CNRS provided with English improvements. All suppori
Neogene
southwestern fauna shows
Turolian
localities
Asia. great along
Kemiklitepe
.-(
A+B (B). In both cases, small
(A) et de Kemiklitepe
a belt from
A+6
mammals
(B). Les micro-mammif6res
Yugoslavia
to Iran
or even
are excluded. sent exclus
to Afghanistan
de ces
(Bonis
et al., 1992). As in many Turolian localities of this socalled “g&co-irano-afghane” bioprovince, the Akkasdagi fauna is dominated by equids and ruminants (figure 3), while the other discrete. Another of small with the generally
and large correlation
large mammalian interest of this
groups remain rather locality is the association
mammals at the same site; this helps of localities where these groups are
separated.
fossil site was reported to us by Osman Nuri YalCin in the winter of 1995 and preliminary work University Research Fund (95.05.01.01) in the same year with the field assistance of Kuddusi finance for excavation of the site and reciprocal visits to the counties. F. Murdoch helped is gratefully acknowledged.
Version abdgee Introduction Les formations n>nes recouvrent une grande partie de l’rlnatolie ; marines 3 Pest et au sud, elles sent continentales en Anatolie centrale, 0iI1 elles se sent accumuEes dans plusieurs bassins. La datation de ces formations continentales est essentielle pour interpreter I’Cvolution tectoniyue de la r@ion. Le vaste bassin de (;ankiri-Corum, situ6 9 l’est d’Ankara @gure I), a IivrC uric douzaine de &alit& de mammiftires qui permettent d’Cbauchcr une stratigraphie du bassin (Sen et al., 1998). La d&ouvefle du riche gisemcnt d’Akkasdagi contribue P la datation de ces terrains continentaux et permet de pri-ciscr nos connaissances sur i’~volution des faunes de mammif+res en Turquie &rant le Mioc2ne sup6rieur.
Tectonique
et stratigraphie
Le soulevement progressif du plateau anatolien durant le i%ogPne :I gPni-r6 sa continentalisation et la formation des bassins iniramonta~neux. don1 les plus importanls sent Its
508
C. R. Acad
bassins de ‘l’uzgblii, Haymana, Cankiri-Gorum et Sivas. Group& sous le nom de sabassins centraux d’Anatolie 1):ils sent, en fait, des aires de subsidence cntrc les blocs continentaux sureleves (Birgili et al., 1975 : G8rCir et al.. 1984 : Cater et al., 1991). I>ans le bassin de Cankiri-@rum. les formations sedimentaires correspondent i trois phases majeures de sedimentation, &par&s par deux discordances angulaires : formations marines &I PaEocene superieur - fioc?ne supf?rieur, formations fiuvio-lacustres (partiellement 6vaporitiques) du Miocene in@ rieur - Mioctine supCrieur et dCp6ts fluviatiles du Mio&ne sup&ieur - f+Xstoc&e (Rirgili et al.. 1975). Le nouveau gisement d’Akkasdagi se trouve clans ce dernier ensemble. Les formations marines datant du I’alPogPne affleurent dans le Norcl et le Centre du bassin. tandis que cellcs du \J6og&w recouvrent les parties centralcs et m&idionales. Ce schema de repartition des unites skdimentaires temoigne d’une migration vers le sud des milieux de dQAt. 12s formations continentales n&xgi?nes sent form&s soub le conlrc^le d’une nhtectonique
Sci. Paris, Sciences
de la terre
et des plan&es
/ Earth & flanefary Sciences 1999.329,503-510
A new Late Miocene
active, qui s’observe partout sur le plateau anatolien. Depuis le Plioc&e, ce bassin est limit6 au nord par la faille nordanatolienne yigure 1). L’activite volcanique existe autour du bassin de Cankiri-$orum depuis l%ocPne, avec un maximum au tours du Mio&ne superieur et du PliocPne. Cependant, les rapports du volcanisme avec la tectonique sont inconnus. Deux vastes complexes volcaniques, ceux de Galatie et de Cappadoce, ont apparemment servi de source pour le remplissage sedimentaire de ce bassin. Le tuf de l’horizon fossilifgre d’Akkasdagi et d’autres d6p6ts volcanoclastiques observCs dans la region sent probablement issus du massif volcanique de Cappadoce.
Lithologie
des formations
fossili@res
Les d6pBts sedimentaires de la region d’Akkasdagi sont rapport& sur les cartes geologiques comme appartendnt A la formation de Kizilirmak dat6e de Miocene superieur (Birgili et al., 1975 ; Seymen, 1982) ou du Mioc?ne moyen (Erdogan et al., 1996), par correlation lithologique avec des unites similaires dans d’autres secteurs du mCme bassin. Dans la region &tudi&, cetle formation recouvre le substratum granitique ou mCtamorphique yigure 1). L’absence des unites sedimentaires plus anciennes est interprCt& comme le r&ultdt d‘une migrdtion des milieux de sedimentation vers le sud au tours du NU&ogt’ne. Akkdsddgi est le relief principal de la region. La jgwe 2 montre la lithologie des sediments sur une coupe type de cette montagne. Les niveaux marquants sent les trois horizons de tufs et les calcaires marneux qui s’intercalent avec des marnes, sables et conglom&ats. Ces derniers sont des depcits de c6nes de dejection, tandis que les calcaires marneux indiquent la p&sence des etendues lacustres d’une certaine duree. Les deux premiers horizons de tufs semblent Cstre des d6p6~5 a&iens. Leur granulometrie est fine et reguliere ; ils contiennent de fins conduits de gaz. tkmoins d’une mise en place de matkriaux chauds, provenant des explosions volcaniques (Case et Wright. 1987). Les tuffkes du troisieme horizon sont trPs altCrts. La source de ces tufs et tuffites esl inconnue. Dam la r&ion. le principal centre volcanique susceptible de fournir ces mat& riaux est le complexe volcanique de Cdppadoce, qui est situ6 2 plus de 100 km.
Faune de mammifkes Les gisements de mammiferes se situent dans le premier niveau de tufs sur les flancs sud-est de la montagne, P 3 km au nord-ouest du village de GBkesme. Les trous form& par 1’6rosion h la surface de ce tuf sont remplis par une matrice volcanoclastique, qui contient d’abondants restes de mammfires. Trois poches fossilifkres ont 6te fouilEes en 1997 ; ils ont livri- des restes de grands et de petits mammif$res. Les os sent souvent prCservCs en connexion. 011 m@me isol& ; la plupdn sont complets. Dans les trois poches fouilEes, la faune est dominee par les P&issodactyles et les Artiodactyles. D’aprks la taille, en par& culier de celle de mPtatarses (L = 236 i 285) et de m&carpes (1. = 185 i 2401, on peut distingler deux, voire trois ep$ces C. R. Acad. Sci. Paris, Sciences 1999 329,503~510
de la terre
et des planGtes
/
mammal
locality
from central
Anatolia
d ‘t-lipparion. Les rhinoc&os sont relativement abondants, d’apriis le nombre 6lev6 d’os de membres r&ok&. Les Artiodactyles sont plus varies, avec quatre genres de Bovidae, deux Gira%dae et un SuidC. Parmi les Bovidae, une gazelle de taille moyenne, avec des chevilles coufles et robustes, ainsi que des premolaires courtes par rapport aux molaires, abonde dans ce gisement. Par ces caract&es, elle differe de Gazellapilgrimi de Samos, de G. cupricornisde Pikermi et de G. deperditadu mont LubCron et de Dtyko, mais ressemble 2 une esp&e i&d&e, deja reconnue h Kemiklitepe A+13 (Bouvrain, 1994). Le genre ProtovX est present, avec un ci%ne juvenile et quatre mschoires superieures ; le degri: d’hypsodontie 6Ev6e des dents se compare P Protoly~ sp. d&crit k Kinik et Kemiklitepe A+B (Kiihler, 1987 ; Bouvrain, 1994). Un maxilaire, avec des dents de dimensions similaires, se compare i Tragoportux rugosifrons de Samos. Enfin, quelques chevilles spiralees peuvent &tre d6termin&s comme etant celles de I?-CJStrepsiceros sp. Des Giraffidae, nous n’avons pu recolter que des OS de membres dont la taille indique la presence de deux genres, probablement Samotberiumet Palaeotragus,d&j8 connus en association 5 Kemiklitepe (Geraads, 1994). Les Suidae sent relativement abondants 2 Akkasdagi. L’absence de pl et la petite taille des canines infirieures permettent d’attribuer ces restes 6 :Micro.~ton~.x mujor, qui est une espece bien connue dans toute 1’Eurasie durant le Turolien. Les Proboscidiens sont represent& par quelques rares specimens determines comme Choerolophodon sp. Les carnivores sont relativement rares. Des fragments de mandibules et des dents isolees d’un petit IIyaenidae peuvent iltre rapport& ;i Huyaenotheritimwon@, en raison de leurs dimensions et de leurs proportions. tine prkmolaire infirieure isolee est semblable 5 celle de Adcrocuta eximia. Ces deux taxons sont frrCquents dans les gisements turoliens de Turquie et de G&e (de Honis, 1994). Ce gisement a livr6 une patte antkrieure et une patte posterieure presque complPtes, appartendnt i Olycbropus gaudryi (Tubulidentata), proche en taiile des specimens de Samos (Colben, 1941). Parmi les restes de petits mammif&es, il est possible d’identifier un Erina&idC Schizogakrix atticus(mandibule et dents isol@es)> deux esp&es de Cricetidae appartenant au genre Byzuntinia (mandibules, maxillaires et dents isolees), mais distinctes par la taille et par la morphologie des molaires, un Muride rep&sent6 par une ml identique ;i celle d’Occitanom.ys prouocatoret,enfin, deux autres dents is&es de Spdlacidae et de Sciuridde.
Conclusions La composition de la faune ici d&rite est voisine de celle des faunes de Kemiklitepe A+B el de Kinik (figure 3), deux localit& situt?es 2 environ 400 km au sud-est d’Akkd&gi et datCes du Turolien moyen (MN12). La plupart des grands mammiferes et. parmi les petits, Schizogabrix attica, B.yzantivia hellenicuset Occitanom.ys prozwator sont dcs elements caractBristiques de cette zone en Turquie er en Gr&c. Lessentiei des taxons de cette faune sont des animaux vivant dans des prairies boiskes, qui constituaienr l’environnement dominant au ‘l’urolien, le long d’une ceinture nomm6e Ccprovince gri-coil-ano-afghane 2’ (de Honis er al., 1092)
Earth& PlanetarySciences
509
N. Kazanci
et al.
La lormation de Kizilirmak, dans laquehe se trouve le gisement d’Akkasdagi, est I’unite sedimentaire k4 phrs etendue du bassin de Cankiri-Corum. &pendant, la succession lithoiogique des sediments 2 Akkasdagi differe de celle de la section type, qui est dominee par des sediments detritiques rouges. La presence des calcaires lacustres a Akkasdagi indiquerait que la
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Kocylgit A., Turkmenoglu A., Beyhan A., Kaymakci N. and Akyol E. 1995. Post-collisional tectonics of Eskisehir-Ankara-Cankiri segment of Izmir-Ankara-Erzincan suture zone: Ankara erogenic phase, Turkish Ass. Petroleum Gee/. Bull., 6, 69-86
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partie sud du bassin se situait plus bas au Miocene superieur que la partic nord, permettant le developpement des lacs et des etangs, tandis que, dans la partie nord, des environnements sedimentaires fluviatiles semblent avoir constitui: I’essentiel des milieux.
Sciences
de
The Cricetodontini Turkey), in: Proc.
la terre
et des
plan&es
havzasinda Congress
tektonik of Turkey,
(Rodentia) from the Bayraktepe Ken. Nederl. Akad. Wetensch.,
1 Earth
N., Seyitoglu of Miocene Basin, central
G. and Sen evaporitic Anatolia,
& Planetary Sciences 1999.329,503-510
des sciences
/ pditions
Palaeontology / PalPontologie (Vertebrate Palaeontology / Pa/&nto/ogie
scientifiques
et mbdicales
Elsevier
SAS. Tous droits
r&sew%
des VertPbr&
Geology of a new Late Miocene in central Anatolia, Turkey
mammal
locality
Gologie d’un nouveau gisement de mammij&es d’dge Mioc&e supkieur en Ana tolie ten trale, Turqu ie Nizamettin Kazancia, Sevket Senb*, Giirol Seyitoglu”, Hakan Araza, Baki VaroY, Levent Karadenizli” a Ankara Universitesi, Fen Fakiiltesi, Jeoloji h Laboratoire de palContologie du Museum c Laboratoire
de palPontologie
des vert&br&
d Laboratoire
de palkontologie
des vertbbr&,
(Received
Abstract
13 April
-
The
1999,
new
accepted
mammal
Miihendisligi BBliimO, 06100 national d’histoire naturelle, et paleontologie Esa 7073
12 July
locality
Louis de Bonisc,
humaine,
du CNRS,
Ankara, Turkey UMR CNRS 8569, universite
universitk
GeneviPve
8, rue Buffon,
de Poitiers,
86022
Pierre-et-Marie-Curie,
Bouvraind,
75005
Poitiers 75252
Paris,
cedex,
Paris cedex
France
France 05, France
1999)
of Akkasdagi
yielded
a rich
fauna
dated
as Middle
Turolian. It is situated in the southern part of the Cankiri-Corum Basin in central Anatolia. In the Akkasdagi area, the sedimentary deposits, mapped as the Kizilirmak Formation, consist of tuffs and lacustrine limestones intercalated with elastic deposits, whilst in its type section, situated deposits. Miocene,
to the north near Kizilirmak town, this formation is mainly formed of fluviatile Facies distribution and geological observations led to conclude that during the depositional centers migrated from the north to the south of this basin.
(0
1999
Acadkmie
Mammal
locality
des sciences
/ Late Miocene
/ iditions
scientifiques
/ stratigraphy
et medicales
/ correlation
Elsevier
SAS.)
/ Anatolia
Ri%umk - Le nouveau gisement de mammif~rcs i Akkasdagi, au sud du bassin de cankirixorum (Anatolie centrale), a livrii une abondante faune dati-e du Turolien moyen. Dans le secteur d’Akkasdagi, la s&ie sedimentaire attribuee a la formation de Kizilirmak comporte une succession de tufs et de calcaires lacustres, intercal& dans les sediments dhitiques. Cette succession diffhe de celle de la coupe type, situ& plus au nerd, qui est domint% par des d6p6ts fluviatiles. Les observations g6ologiques montrent qu’au tours du Mioche, le centre de s6dimentation a migri- du nord vers le sud. (0 1999 AcadPmie des sciences / fiditions scienlifiques et medicales Elsevier SAS.) gisement
de MammiEres
/ Miocene
suph-ieur
/ stratigraphie
/ corriAation
/ Anatolie
Version abregee (voir p. 508) 1. Introduction parts The principal aim of this paper is to present a newly discovered Late Miocene mammal locality (Akkasdagi) and its geological context. This work is part of an integrated geological study of Neogene deposits in the Cankiri-Corum Basin. Neogene deposits cover the major Note
pr&entCe
* Correspondence
par Philippe and
reprints.
de la terre
et des plan&es
/ f&h
Anatolian
ing the Late Cenozoic they record all tectonic
Taquet.
Sci. Paris, Sciences 1999.329,503-510
C. R. Acad.
of the
peninsula.
central and western Anatolia, and southern Anatolia. The times larger than the marine,
& Planefory
Sciences
They
are
terrestrial
in
but mainly marine in eastern terrestrial cover, which is 4-5 is of great interest for study-
tectonic phases
evolution and events.
of Turkey, A good
since under-
N. Kazanci et al. standing of their chronology is essential to interpret tectonic events and to construct basin evolution models. In central Anatolia, Early Miocene deposits are mainly lacustrine while the Middle-Late Miocene ones are mainly palustrine and fluviatile (LOttig and Steffens, 1976). The stratigraphy of these continental deposits is not yet well established, mainly because of (1) the presence of many small sedimentary basins with unclear borders, and (2) the frequent lateral facies changes in their deposits. Palaeontological research in these deposits are not extensive enough to build a detailed biostratigraphy of terrestrial deposits and to provide correlation between the lithologic units. The available stratigraphy of the central Anatolian basins is based at present on the geometric relationshipsof lithological unitsand on a few mammalian faunas. In the Cankiri-Corum Basin, a dozen mammal localities are already known (Sen et al., 1998), but they are situated in its northern and central parts, while the Akkasdagi locality is near the southern edge of this basin. As stressed in this paper, the present data are far from establishing a detailed stratigraphy of Neogene deposits. Consequently, all newly discovered mammal localities contribute to refining the current stratigraphic chart. The Akkasdagi mammal locality is situated in the southern part of the Cankirixorum Basin, NNW of Kaman town and some 3.5 km from GGkesme village (figure 7). Bones are concentrated on a thick tuff layer along the southwestern slopes of the hill, Akkasdagi.
2. Tectonic
setting and stratigraphy
The closure of the northern branch of Neotethys during the Late Cretaceous-Late Eocene created a complex tectonic pattern (Sengcir and Yilmaz, 1981; Seng6r and Natal’in, 1998). The closure occurred between irregular margins, therefore the evolutionary history of basins, including Cankiri-Corum Basin, is not correlative from one area to another (G&iir et al., 1984; Cater et al., 1991; Tiiystiz and Dellaloglu, 1992; Erdogan et al., 1996). Even within the Cankiri-Corum Basin, tectonic phases and structures in different subbasins show great differences (figure 7). Such a complex evolution led geologists to contradictory interpretations (Koc;yigit, 1991; TOysLiz and Dellaloglu, 1992; Erdogan et al., 1996; Seyitoglu et al., 1997). The progressive uplift of the Anatolian peninsula during the Miocene generated its continentalization, thus forming an intramontane plateau in central Anatolia. The origin of the present-day morphological features of the Anatolian plateau should thus be regarded as undergoing its tectonic evolution during the Neogene period (G&Or et al., 1995). The depression areas grouped under the name of Inner Anatolian Basins are in fact composed of the Cankiri-Corum, Tuzgiilti, Haymana and Sivas basins (figure I) which are the subsidence areas between the uplifted continental blocks (Birgili et al.,1 975; G&Or et al., 1984; Cater et al., 1991).
504
The Cankiri-corum Basin is filled with deposits ranging in age from Late Paleocene to Pleistocene. Three main periods of sedimentation are separated by two major angular unconformities: Late Paleocene-Late Eocene marine deposits, Early-Late Miocene fluviolacustrine (partly evaporitic) deposits, and Late Miocene-Pleistocene fluviatile deposits (Birgili et al., 1975). The earliest marine deposits crop out in the central and northern parts of the basin, while the later deposits are mainly exposed in the central and southern regions. This distributional pattern might be indicative of a southern shift of depositional centers. The uppermost continental deposits are formed under the control of active neotectonics that are encountered almost everywhere in the Anatolian plateau. Since the Pliocene, this basin has been bordered to the north by the North Anatolian transform fault (figure I). The contribution of volcanic products in the filling of the Cankiri-Corum Basin is known to have existed since the Eocene, with a maximum during the Late MiocenePliocene interval. The relationships of the tectonic dynamics in Cankiri-Corum Basin with the volcanic activity are unknown. However, this basin is surrounded, and even partly covered in the north, by two vast volcanic complexes, the Galatia and Cappadochia volcanic complexes. These volcanic complexes are in turn one of the main source areas for sediments infilling the Cankiri-Gorum Basin. The mammal-bearing tuff horizon at Akkasdagi and its surrounding areas probably originated from the northwestern edge of the Cappadocian volcanic complex. In summary, the Cankiri-Corum Basin developed during Late Paleocene to Oligocene under the postcollisional compressive tectonic regime (Tiiysiiz and Dellaloglu, 1992; Erdogan et al., 1996), which divided the basin into smaller subbasins in the Middle Eocene-Oligocene (Karadenizli et al., 1998). However, the tectonic style of Miocene-Quaternary evolution of the basin is a subject of current debate (Kocyigit et al., 1995; Seyitoglu et al., 1997).
3. Lithology sequence
of the fossiliferous
In the southern part of Cankiri-Corum Basin, Late Miocene deposits cover the metamorphic basement (Kirsehir Massif; Seymen, 1982), the granites which cut this massif, or the marine Eocene deposits. In the Akkasdagi area, Neogene deposits unconformably overlie the basement formed of granites, ophiolites and metamorphic rocks. The absence of older sedimentary rocks in the Cankiri-Corum Basin implies that the sedimentary units in the Akkasdagi area are an overlap following the southwestern development of this basin. The sedimentary deposits of the Akkasdagi area are mapped as Kizilirmak Formation dated as Late Miocene (Birgili et al., 1975; Seymen, 1982). However, Erdogan et al. (1996) proposed, by lithological correlation with similar deposits of the Cankiri-Gorum Basin, a Middle Miocene age, and considered them as ‘cover deposits’.
C. R. Acad. Sci. Paris, Sciences
de la terre
et des plan&es
/ Eatih
& Planetary Sciences 1999.329,503-510
A new
Figure 1. Simplified geoiogical map of north 2. Pontid block. 3. Sakarya block. 4. Calatia Carte geologique simplifiee 1. Bassins neogenes. 2. Bloc 7. ChaFne de Taurus.
de I’Anatolie de Pontides.
Sciences
de
nord-centrale et localisation 3. Bloc de Sakarya. 4. Complexe
la terre
Miocene
mammal
locality
from
central Anatolia with the main tectonostratigraphic units and Neogene basins. volcanic complex. 5. Ophiolitic formations. 6. Kirsehir Massif. 7. Taurus belt. des principales volcanique
The Akkasdagi fossiliferous horizon is a part of a Messa type hill which is about 2.5 km long in the NE-SW direction, and 1 km wide. Akkasdagi forms the major relief of the area and is highly visible because of its relief and light colour of sediments in contrast to the surrounding red, steppe landscape. The top of the hill is at 1 019 m altitude. The nearest village, Cokesme, is situated about 3 km southeast of the hill. The bone-bearing sites are along its soutwestern slopes at an altitude of 950 m (coordinates X = 4372500, Y = 0556000). figure 2 presents the typical lithological succession of the Akkasdagi deposits. Three noticable volcanoclastic horizons are intercalated in marls and clayey limestones capped by coarse elastic sediments. Conglomeratic lenses are quite frequent in levels above the fossiliferous tuffs, C. R. Acad. Sci. Paris, 1999 329,503~510
Late
et des
pIaWes
/ Earth
unites de Calatie.
tectonostratigraphiques 5. Formations ophiolitiques.
et des
central
Anatolia
1. Neogene
bassins 6. Massifde
basins.
neogenes. Kirsehir.
and lateral facies changes between clayey, marly, sandy and conglomeratic layers are also observed. These are interpreted as alluvial fans. The carbonate-rich clays of the lower part display a reddish colour because of oxidation. They also show nodular structures and frequent rootmarks in some horizons, probably indicative of shallow lacustrine depositional environments. The two lower volcanoclastic horizons are composed of fine-grained tuffs, while the third one is a coarse tuftit. The tuffs include gas segregation pipes which imply hot setting of the material (Gas and Wright, 1987). They do not show any clear lithification or graded bedding. Their thickness varies from 3 to 7 m (figure2). Their thickness and morphology indicate that they were settled as nyroclastic flow & hnetary
Sciences
N. Kozanci
et al
ulty of Sciences, studied the stratigraphy of the area and unearthed a reliable collection of mammals from Akkasdagi. in September 1997, the authors of this paper excavated three spots (labelled as AKA, AKB and AKK) along the same horizon to collect mammalian remains and taphonomic observations. We must stress that this mammal locality may disappear, or at least be severely damaged, if the project of an industrial company for exploitation of this tuff for cement row material is realized. The mammalian fauna presented below is based on the material collected between 1995 and 1997. Bones are accumulated in holes that are apparently dug out by erosion of the tuff surface; they are at most 1 m deep and 2 m wide. The matrix of fossilifereous pockets is also the tuff mixed with some elastic elements. The three bone pockets excavated in 1997 contain both large and small mammals. Among the large mammals, the perissodactyls and especially hipparions are predominant. They are represented by many skeletal remains often in connection, limb and cranial bones. The main part of specimens is not yet prepared; it is therefore not possible to determine them at the species level. Nevertheless, it seems that two species, perhaps three, are differentiated by size. Thus, the length of the third metatarsal varies from 236 to 285 mm and that of the third metacarpal from 185 to 240 mm. A rhinoceros is represented by some limb bones in all three bone pockets. The artiodactyls, although numerically less than the perissodactyls, are more varied since they include bovids, giraffids and suids. There are four bovid genera. The most abundant is a gazelle whose remains (cranium, horn cores, jaws) have been recorded from the three fossiliferous spots. It is a middle-sized species with short and robust horn cores (length between 8 and 12 cm), and with deep grooves especially on their posterior face. The premolars are rather short compared to the molars. The horn cores of this gazelle differ from that of Gaze/la pilgrimifrom Samos (Greece) in being shorter and strongly curved, from Gaze//a capricornis from Pikermi (Greece) by their mediolateral compression, and from Gaze/la deperdita from Mont Luberon (France) and Dytiko (Greece) in being less curved backward. This species is quite similar to that of Kemiklitepe A + B (Turkey; Bouvrain 1994). A juvenile skull fragment (from the pocket AKK) and four upper jaws (AKB) belong to the genus Protoryx. Beyond the generic characters of Protoryx (straight horn cores, large sinus extending into the pedicel, short premolars, molars with strong and pinched styles) the most striking feature of Protoryx from Akkasdagi is the strong hypsodonty (hypsodonty index of M3 - between 118-l 25) exceeding for example that of Protoryx from Maragha (Iran). Inversely, Protoryx from Kinik (Turkey; Kijhler, 1987) and from the upper levels of Kemiklitepe are quite comparable to the Akkasdagi specimens. The tribe Boselaphini, usually abundant in Eurasian Late Miocene localities, is very rare in Turkey, An upper jaw from AKB can be referred to a Tragoportax similar in size to T rugosifrons from Samos with however rather long
m 70
red Clastics
white clayey Limestones
brownish 30
grey Tuffites
grey Marls grey Tuffs
10
-MAMMALIAN FAUNA plnkish white Tuffs unconformity
Pre Neogene Figure 1 ithologie kasdagi.
2. Lithology des
of late
sediments
Miocene
deposits
du Miocene
sup&rieur
basement at Akkasdagi dans
section.
la coupe
d’Ak-
(Cas and Wright, 1987). The tuffits of the third volcanoelastic level are quite weathered. The source area of tuffs, and tufits is not yet known. There are two close andesitic outcrops to the northeast and southeast of Akkasdagi. Moreover, trachyte and rhyolite outcrops are located west of Kaman. Even though rnore detailed studies are needed to locate the source area, we hypothesize that these tuffs originated from these volcanics which belong to northwestern edge of Cappadocidn volcanic complex.
4. Mammal
fauna
This mammal locality was indicated to one of us (N.K.) by a villager. Later on our investigations revealed that it was already known, but not explored, by palaeontologists. In his PhD thesis Ozansoy (1958) notes that “Dr. Burchart recently discovered a fauna with Hipparion gracile at Kaman”. Ayan (1963), when studying the petrography of different formations in the Kaman area, rediscovered this locality, and he illustrated some specimens as Hipparion grab/e. The locality was visited by E. Heintz on 21 October 1971; he collected 229 specimens, preserved in the Natural History Museum of Paris. During the 1995-l 996 field seasons, geologists from the Ankara University, Fac-
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et des
plan&es
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& Planetary Sciences 1999.329.503-5 10
A new
premolars. Tragoportax has not been found at Kemiklitepe, but it was mentioned at Kinik (K6hler, 1987). An antelope with spiral horn cores, assigned to Prostrepsiceros, is represented by a frontlet (AKK) and a partial horn core (AKB). It resembles frostrepsiceros rotundicornis from Pikermi in not having a transverse compression on the horn core, but it differs in having a deep anteromedial groove. Such a groove is known on horn cores of F! libycus from Sahabi (Libya) that is however a little larger in size (Lehmann and Thomas, 1987). The genus Prosfrepsiceros is rare in Turkey; nevertheless Senyiirek (1952) illustrated two horn cores from GBkdere. This genus is absent both at Kinik and Kemiklitepe. Giraffid remains are rare, only some limb bones were found in the three bone pockets. According to their size they could belong to a Samotherium, quite similar to that of Kemiklitepe A+B (Geraads 1994). However a phalanx and a fragment of calcaneum from AKK are clearly smaller and could be assigned to a Palaeotragus. Suids are relatively abundant and represent the genus Microstonyx, which is the most widespread form both in Europe and central Asia during the Late Miocene. The lack of pl as well as the small size of the lower canine allow it to be determined as M. major. We must also mention the presence of a few proboscidian remains determined as Choerolophodon sp. The carnivora are present with two species of hyaenids. One of them, Hyaenothedum wongi, is represented by several specimens of isolated teeth and fragments of mandibles belonging to three different individuals. The size and proportions of teeth are similar to those of the specimens recovered from the Kemiklitepe locality in western Turkey (de Bonis, 1994). A large isolated lower premolar looks like those of small individuals of Adcrocuta eximia. It can be identified as A. cf. eximia. Aardvark remains were found in the spot AKK with a left manus and a right pes. In size, this animal is similar to Orycteropus gaudryi Major, 1888 from Samos (Mclll length = 46.5, Mtlll length = 69.2). Aardvarks are quite common in Middle-Late Miocene localities in Turkey and Greece (Colbert, 1941; Sen, 1994). This locality has also yielded small mammals in all three spots excavated. Some remains were collected during the 1997 excavations, while some others were obtained by sorting the residue after wet screening. We have to note that the tuff is hard to break up in water and to concentrate. A mandible and some isolated lower teeth belonging to an erinaceid insectivore were determined as Schizogalerix atticus (Rtimke, 1976). On ml and m2, the trigonid valley is narrow and deep, the posterior arm of the hypoconid is connected to the entoconid but not to the posterolophid. These characters are typical for S. attica from Chomateri (Greece), and the size of the Akkasdagi specimens also fits with this species. It seems that this genus has, in the Aegean area, an anagenetic evolution since only one lineage is recognized from the Early Astaracian (Pasalar, S. pasalarensis Engesser, 1980) to Latest Turolian (Amasya, Shizogalerix n. sp. , in Engesser, 1980). C. R. Acad Sci. Paris, Sciences 1999.329.503-510
de la terre
et des plan&es
/ farfh
Late Miocene
mammal
locality
from
central
Anatoiia
Among rodents, the family Cricetidae is present with two species of Byzantinia well distinguished in size and morphology. The largest form (Ml = 3.75 x 2.70 mm) is quite similar to B. hellenicus (Freudenthal, 1970) from Samos in having Ml widened, with a strong anterolabial spur and well developed ectolophs. The second form is smaller, Ml (3.45 x 2.25) without spur and with lower ectolophs. This second species is smaller than the previous one but larger than any other species of Byzantinia from the Late Miocene of Turkey and Greece (Bruijn, 1976; Unay, 1980). It is for instance determined as Byzantinia sp, The genus Byzantinia has been known in Turkey and Greece since the late Astaracian and it disappears towards the end of the Turolian. The paucity of the knowledge on its Late Miocene, mainly Turolian representatives means that its discovery in Akkasdagi is of great interest. Only one ml (I .88 x 1.22) of Muridae has been found at the spot AKK. Its dimensions, the presence of a small anteromedian cuspid and a wide posterior edge allow its comparison with Occitanomys provocator Bruijn, 1976 from Chomateri and Samos 53 (Greece, MN1 2). A worn M3 (2.04 x 2.42) and a damaged Ml (1.97 x 2.59) can only be determined as Spalacidae indet. and Sciuridae indet., respectively. Concerning the large mammals, the composition of the Akkasdagi fauna is similar to that of the upper level of Kemiklitepe or that of Kinik (figure 3), and indicates therefore a Middle Turolian age (MNI2). Among the small mammals, the characteristic taxa (Schizogalerix, Byzantinia and Occitanomys) are all previously known from the Middle Turolian localities in Greece (Chomateri and Samos S3). Some K/Ar and Ar/Ar ages are also available for the locality Samos S3 which is bracketed between two tuff horizons dated as 7.28 + 0.01 and 7.09 + 0.01 Ma respeclively (Swisher, 1996). These similarities are strong enough to date the Akkasdagi fossiliferous horizon as MN1 2.
5. Conclusions Kizilirmak Formation is the most extensive Late Miocene unit of Cankiri-Corum Basin. In its type locality, it is composed of red coloured and dominantly coarse elastics which are covered by gypsum deposits. The Akkasdagi area is also mapped as Kizilirmak formation (Birgili et al., 1975; Seymen, 1982) though the sedimentary unit in the study site is rather different from the type locality since it includes a carbonate-dominated palustrine sequence with volcanoclastic layers. A red elastic sequence similar to the type location of Kizilirmak Formation is observed on the uppermost levels of the Akkasdagi section (figure 2). Such a lithofacies distribution may indicate that the southern part of the basin was a relatively lower area with swamps and/or shallow lakes, while fluviatile environments predominated in the northern parts during the Late Miocene. Later, swamps and lakes moved toward the north, and the Akkasdagi area became purely terrestrial. Similar changes & Planetary
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507
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et al
rrrrrr r ,*R?‘“r+rpL+
Figure +:>>.
3. Comparison
of the fauna1 composition
Comparaison diagrammes.
de la composition
or migrations
of depositional
whole central al., 1995).
Anatolia
The Akkasdagi of open woodland
resemblances
with
the
those
des gisements
environments
that
were
(A) with
d’Akkasdagi
typical
in
(G&Or
et
assemblage is characteristic were dominant during
the
throughout
mammalian habitats
Turolian in southeastern The composition of
faunique
of Akkasdagi
the
Europe and Akkasdagi of other
Acknowledgements. The Akkasdagi was done with the support of Ankara Karakus. TUBITAK and CNRS provided with English improvements. All suppori
Neogene
southwestern fauna shows
Turolian
localities
Asia. great along
Kemiklitepe
.-(
A+B (B). In both cases, small
(A) et de Kemiklitepe
a belt from
A+6
mammals
(B). Les micro-mammif6res
Yugoslavia
to Iran
or even
are excluded. sent exclus
to Afghanistan
de ces
(Bonis
et al., 1992). As in many Turolian localities of this socalled “g&co-irano-afghane” bioprovince, the Akkasdagi fauna is dominated by equids and ruminants (figure 3), while the other discrete. Another of small with the generally
and large correlation
large mammalian interest of this
groups remain rather locality is the association
mammals at the same site; this helps of localities where these groups are
separated.
fossil site was reported to us by Osman Nuri YalCin in the winter of 1995 and preliminary work University Research Fund (95.05.01.01) in the same year with the field assistance of Kuddusi finance for excavation of the site and reciprocal visits to the counties. F. Murdoch helped is gratefully acknowledged.
Version abdgee Introduction Les formations n>nes recouvrent une grande partie de l’rlnatolie ; marines 3 Pest et au sud, elles sent continentales en Anatolie centrale, 0iI1 elles se sent accumuEes dans plusieurs bassins. La datation de ces formations continentales est essentielle pour interpreter I’Cvolution tectoniyue de la r@ion. Le vaste bassin de (;ankiri-Corum, situ6 9 l’est d’Ankara @gure I), a IivrC uric douzaine de &alit& de mammiftires qui permettent d’Cbauchcr une stratigraphie du bassin (Sen et al., 1998). La d&ouvefle du riche gisemcnt d’Akkasdagi contribue P la datation de ces terrains continentaux et permet de pri-ciscr nos connaissances sur i’~volution des faunes de mammif+res en Turquie &rant le Mioc2ne sup6rieur.
Tectonique
et stratigraphie
Le soulevement progressif du plateau anatolien durant le i%ogPne :I gPni-r6 sa continentalisation et la formation des bassins iniramonta~neux. don1 les plus importanls sent Its
508
C. R. Acad
bassins de ‘l’uzgblii, Haymana, Cankiri-Gorum et Sivas. Group& sous le nom de sabassins centraux d’Anatolie 1):ils sent, en fait, des aires de subsidence cntrc les blocs continentaux sureleves (Birgili et al., 1975 : G8rCir et al.. 1984 : Cater et al., 1991). I>ans le bassin de Cankiri-@rum. les formations sedimentaires correspondent i trois phases majeures de sedimentation, &par&s par deux discordances angulaires : formations marines &I PaEocene superieur - fioc?ne supf?rieur, formations fiuvio-lacustres (partiellement 6vaporitiques) du Miocene in@ rieur - Mioctine supCrieur et dCp6ts fluviatiles du Mio&ne sup&ieur - f+Xstoc&e (Rirgili et al.. 1975). Le nouveau gisement d’Akkasdagi se trouve clans ce dernier ensemble. Les formations marines datant du I’alPogPne affleurent dans le Norcl et le Centre du bassin. tandis que cellcs du \J6og&w recouvrent les parties centralcs et m&idionales. Ce schema de repartition des unites skdimentaires temoigne d’une migration vers le sud des milieux de dQAt. 12s formations continentales n&xgi?nes sent form&s soub le conlrc^le d’une nhtectonique
Sci. Paris, Sciences
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et des plan&es
/ Earth & flanefary Sciences 1999.329,503-510
A new Late Miocene
active, qui s’observe partout sur le plateau anatolien. Depuis le Plioc&e, ce bassin est limit6 au nord par la faille nordanatolienne yigure 1). L’activite volcanique existe autour du bassin de Cankiri-$orum depuis l%ocPne, avec un maximum au tours du Mio&ne superieur et du PliocPne. Cependant, les rapports du volcanisme avec la tectonique sont inconnus. Deux vastes complexes volcaniques, ceux de Galatie et de Cappadoce, ont apparemment servi de source pour le remplissage sedimentaire de ce bassin. Le tuf de l’horizon fossilifgre d’Akkasdagi et d’autres d6p6ts volcanoclastiques observCs dans la region sent probablement issus du massif volcanique de Cappadoce.
Lithologie
des formations
fossili@res
Les d6pBts sedimentaires de la region d’Akkasdagi sont rapport& sur les cartes geologiques comme appartendnt A la formation de Kizilirmak dat6e de Miocene superieur (Birgili et al., 1975 ; Seymen, 1982) ou du Mioc?ne moyen (Erdogan et al., 1996), par correlation lithologique avec des unites similaires dans d’autres secteurs du mCme bassin. Dans la region &tudi&, cetle formation recouvre le substratum granitique ou mCtamorphique yigure 1). L’absence des unites sedimentaires plus anciennes est interprCt& comme le r&ultdt d‘une migrdtion des milieux de sedimentation vers le sud au tours du NU&ogt’ne. Akkdsddgi est le relief principal de la region. La jgwe 2 montre la lithologie des sediments sur une coupe type de cette montagne. Les niveaux marquants sent les trois horizons de tufs et les calcaires marneux qui s’intercalent avec des marnes, sables et conglom&ats. Ces derniers sont des depcits de c6nes de dejection, tandis que les calcaires marneux indiquent la p&sence des etendues lacustres d’une certaine duree. Les deux premiers horizons de tufs semblent Cstre des d6p6~5 a&iens. Leur granulometrie est fine et reguliere ; ils contiennent de fins conduits de gaz. tkmoins d’une mise en place de matkriaux chauds, provenant des explosions volcaniques (Case et Wright. 1987). Les tuffkes du troisieme horizon sont trPs altCrts. La source de ces tufs et tuffites esl inconnue. Dam la r&ion. le principal centre volcanique susceptible de fournir ces mat& riaux est le complexe volcanique de Cdppadoce, qui est situ6 2 plus de 100 km.
Faune de mammifkes Les gisements de mammiferes se situent dans le premier niveau de tufs sur les flancs sud-est de la montagne, P 3 km au nord-ouest du village de GBkesme. Les trous form& par 1’6rosion h la surface de ce tuf sont remplis par une matrice volcanoclastique, qui contient d’abondants restes de mammfires. Trois poches fossilifkres ont 6te fouilEes en 1997 ; ils ont livri- des restes de grands et de petits mammif$res. Les os sent souvent prCservCs en connexion. 011 m@me isol& ; la plupdn sont complets. Dans les trois poches fouilEes, la faune est dominee par les P&issodactyles et les Artiodactyles. D’aprks la taille, en par& culier de celle de mPtatarses (L = 236 i 285) et de m&carpes (1. = 185 i 2401, on peut distingler deux, voire trois ep$ces C. R. Acad. Sci. Paris, Sciences 1999 329,503~510
de la terre
et des planGtes
/
mammal
locality
from central
Anatolia
d ‘t-lipparion. Les rhinoc&os sont relativement abondants, d’apriis le nombre 6lev6 d’os de membres r&ok&. Les Artiodactyles sont plus varies, avec quatre genres de Bovidae, deux Gira%dae et un SuidC. Parmi les Bovidae, une gazelle de taille moyenne, avec des chevilles coufles et robustes, ainsi que des premolaires courtes par rapport aux molaires, abonde dans ce gisement. Par ces caract&es, elle differe de Gazellapilgrimi de Samos, de G. cupricornisde Pikermi et de G. deperditadu mont LubCron et de Dtyko, mais ressemble 2 une esp&e i&d&e, deja reconnue h Kemiklitepe A+13 (Bouvrain, 1994). Le genre ProtovX est present, avec un ci%ne juvenile et quatre mschoires superieures ; le degri: d’hypsodontie 6Ev6e des dents se compare P Protoly~ sp. d&crit k Kinik et Kemiklitepe A+B (Kiihler, 1987 ; Bouvrain, 1994). Un maxilaire, avec des dents de dimensions similaires, se compare i Tragoportux rugosifrons de Samos. Enfin, quelques chevilles spiralees peuvent &tre d6termin&s comme etant celles de I?-CJStrepsiceros sp. Des Giraffidae, nous n’avons pu recolter que des OS de membres dont la taille indique la presence de deux genres, probablement Samotberiumet Palaeotragus,d&j8 connus en association 5 Kemiklitepe (Geraads, 1994). Les Suidae sent relativement abondants 2 Akkasdagi. L’absence de pl et la petite taille des canines infirieures permettent d’attribuer ces restes 6 :Micro.~ton~.x mujor, qui est une espece bien connue dans toute 1’Eurasie durant le Turolien. Les Proboscidiens sont represent& par quelques rares specimens determines comme Choerolophodon sp. Les carnivores sont relativement rares. Des fragments de mandibules et des dents isolees d’un petit IIyaenidae peuvent iltre rapport& ;i Huyaenotheritimwon@, en raison de leurs dimensions et de leurs proportions. tine prkmolaire infirieure isolee est semblable 5 celle de Adcrocuta eximia. Ces deux taxons sont frrCquents dans les gisements turoliens de Turquie et de G&e (de Honis, 1994). Ce gisement a livr6 une patte antkrieure et une patte posterieure presque complPtes, appartendnt i Olycbropus gaudryi (Tubulidentata), proche en taiile des specimens de Samos (Colben, 1941). Parmi les restes de petits mammif&es, il est possible d’identifier un Erina&idC Schizogakrix atticus(mandibule et dents isol@es)> deux esp&es de Cricetidae appartenant au genre Byzuntinia (mandibules, maxillaires et dents isolees), mais distinctes par la taille et par la morphologie des molaires, un Muride rep&sent6 par une ml identique ;i celle d’Occitanom.ys prouocatoret,enfin, deux autres dents is&es de Spdlacidae et de Sciuridde.
Conclusions La composition de la faune ici d&rite est voisine de celle des faunes de Kemiklitepe A+B el de Kinik (figure 3), deux localit& situt?es 2 environ 400 km au sud-est d’Akkd&gi et datCes du Turolien moyen (MN12). La plupart des grands mammiferes et. parmi les petits, Schizogabrix attica, B.yzantivia hellenicuset Occitanom.ys prozwator sont dcs elements caractBristiques de cette zone en Turquie er en Gr&c. Lessentiei des taxons de cette faune sont des animaux vivant dans des prairies boiskes, qui constituaienr l’environnement dominant au ‘l’urolien, le long d’une ceinture nomm6e Ccprovince gri-coil-ano-afghane 2’ (de Honis er al., 1092)
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et al.
La lormation de Kizilirmak, dans laquehe se trouve le gisement d’Akkasdagi, est I’unite sedimentaire k4 phrs etendue du bassin de Cankiri-Corum. &pendant, la succession lithoiogique des sediments 2 Akkasdagi differe de celle de la section type, qui est dominee par des sediments detritiques rouges. La presence des calcaires lacustres a Akkasdagi indiquerait que la
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_--..-.~.- .._- -- .--.....
Birgili S., Yoldas R. and Unalan G. 1975. nin jeolojisi ve petrol olanaklar, Geological fxpl. Res. inst. (MTAj, Rep. No: 5621, Ankara
partie sud du bassin se situait plus bas au Miocene superieur que la partic nord, permettant le developpement des lacs et des etangs, tandis que, dans la partie nord, des environnements sedimentaires fluviatiles semblent avoir constitui: I’essentiel des milieux.
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