new insights on the antalya nappes in the apex of the isparta angle: the isparta �ay unit...

GEOLOGICAL JOURNAL

Geol. J. 38: 283–293 (2003)

Published online in Wiley InterScience (www.interscience.wiley.com). DOI: 10.1002/gj.956

New insights on the Antalya Nappes in the apex ofthe Isparta Angle: the Isparta Cay unit revisited

BRUNOVRIELYNCK1*,MICHELBONNEAU2,TANIELDANELIAN1,JEAN-PAULCADET2 andANDRE¤ POISSON3

1Universite Pierre et Marie Curie, Departement Geologie des bassins sedimentaires, Paris, France2Universite Pierre et Marie Curie, Departement Geotectonique, Paris, France3Universite Paris-Sud, Departement des Sciences de la Terre, Orsay, France

The Isparta Cay unit was defined in the valley of the Isparta Cay (river) as one of the units that constitutes the Antalya Nappes.Situated structurally between the Bey Daglar� autochthon and the Miocene neo-autochthon, the Isparta Cay unit provides deci-sive arguments with respect to the timing of emplacement of deep basinal units, cropping out in the central part of the IspartaAngle, as well as for a model of reconstruction of the Pamphylian Basin, located to the south of the Taurus belt. The Isparta Cayunit (previously named ‘Isparta Cay formation’) consists of a pile of thrust sheets all of which display the following basic sedi-mentary sequence: Triassic marls and sandstones containing plant remains and limestones with Halobia, overlying Jurassic toCretaceous deep-sea sedimentary rocks (radiolarites). Detailed mapping, combined with new and revised stratigraphic data,confirms the existence of a very complex pile of tectonic, rather thin sheets. The basic sequence is composed, from bottomto top, of the following sedimentary units: (1) marls and turbiditic sandstones rich in plant debris; (2) limestones interbeddedwith marls and; (3) regularly-bedded cherty limestones. These three lower units contain rather abundant fossils (i.e. Halobia andammonites) and are Triassic in age: (4) lenticular calcareous breccia in which Middle Jurassic foraminifera are found; (5) radi-olarites, green and then red, including lenticular beds of reworked calcareous sands (now dolomitized and/or silicified). Theradiolarians from the red radiolarites establish a Jurassic to Early Cretaceous age and; (6) red silts and clays with interbeddedcalcareous breccia, which are probably Cretaceous in age. The total thickness of the basic sequence as described above variesbetween 100 and 150 m, depending on the thickness of the lenticular breccia intercalations.

Such a sequence is frequent in the Antalya Complex as one of the deep basinal sequences. It has been interpreted as onesequence expelled from the Pamphylian Basin, located between the Anamas–Akseki platform (Western Taurus) to the NE,and the Bey Daglar� platform to the SW. The age of the radiolaritic sequences of the Antalya Nappes, extended to all the unitsof SW Turkey, is discussed. Copyright # 2003 John Wiley & Sons, Ltd.

Received 15 Ocober 2001; revised version received 5 February 2003; accepted 7 February 2003

KEY WORDS Turkey; Isparta Angle; Antalya Nappes; Triassic; Jurassic; Cretaceous; radiolarites

1. INTRODUCTION

In the central and eastern Mediterranean area, the Mesozoic palaeogeographical setting was dominated by carbo-

nate platforms separated by more or less deep basins. These basins were initiated at various periods and their infill

reflects the sedimentary conditions prevailing within. On the basis of these global palaeogeographical domains, the

Lycian and Antalya nappes comprise roughly three types of units (or nappes): (i) ophiolites (mainly peridotites

and gabbros), representing remnants of an oceanic crust; (ii) shallow-marine platform carbonates (Gavrovo-Tri-

politza and Apulian platforms in the Hellenides; Menderes Massif, Bey Daglar� and Taurus in the Taurides); (iii)

basinal sequences with, in places, volcanic intercalations (Pindos trough, Ionian trough, Pamphylian Basin).

Copyright # 2003 John Wiley & Sons, Ltd.

* Correspondence to: B. Vrielynck, CNRS (FRE 2400), Universite Pierre et Marie Curie, Departement Geologie des bassins sedimentaires, case117, place Jussieu, 75252 Paris cedex 05, France. E-mail: [email protected]

Large-scale palaeogeographical reconstructions have been proposed since Biju-Duval et al. (1977); the latest ones

have been elaborated by Robertson et al. (1996) and by the Peri-Tethys Programme (Dercourt et al. 2000). These

reconstructions have to be considered as hypotheses which can be updated with new data sets, as it is one of the

objectives of our project of correlations in the Aegean area.

In order to simplify the rather complicated terminology used to refer to tectonic units in the Antalya area, we

choose to use here the term ‘Antalya Nappes’ for the allochthonous units thrust onto the Tauride platforms during

the Late Cretaceous to Palaeocene closure of the Pamphylian Basin. These nappes include deep basinal (mainly

sedimentary) sequences, expelled from the Pamphylian Basin, which are tectonically associated with ophiolites.

The term ‘Antalya Complex’ is used here, as suggested by Robertson (1993), for all the imbricate tectonic units of

the central part of the Isparta Angle as they crop out at the present. These units include the ‘Antalya Nappes’

(Late Cretaceous–Palaeocene), and their initial autochthon represented by thick slices of Tauride platforms

(mainly the Bey Daglar�). The ‘Antalya Complex’ resulted from an out-of-sequence thrust dated initially as Late

Miocene (Poisson 1977), but now (Poisson et al. 2003) we know that Middle Pliocene sediments are affected by

this tectonic event (Aksu Thrust). As a result, in the ‘Antalya Complex’ the ophiolites, the carbonate platforms and

the deep basinal units were tectonically imbricated together during Late Miocene–Middle Pliocene times. This

tectonic event corresponds to the last stage of collision between the Anatolian block—represented here by its

southern margin, the Tauride belt—and the Bey Daglar� block. When the Pamphylian Basin closed, the Isparta

Angle was created. At the apex of this angle, the site of Isparta Cay is important as it provides evidence for the

chronology of emplacement of the allochthons—the Antalya and the Lycian nappes, respectively—during the

early Middle Miocene (Langhian) (Poisson 1977).

In the Isparta Cay section the Triassic limestones and radiolarites were recognized as a typical unit of the Anta-

lya Nappes (Gutnic and Poisson 1970). Given the abundance of Triassic macrofossils (Halobia, Ammonitidae and

Aulacoceratidae), and the absence, at the time, of other age diagnostic fossils, the Isparta Cay unit was described at

first as a single series of Late Triassic age: the so-called ‘Isparta Cay formation’ (Dumont et al. 1972; Allasinaz

et al. 1974; Poisson 1977; Gutnic et al. 1979). In this ‘formation’ only the Triassic members were dated (Halobia

limestones, sandstones and marls). Initial radiolarian ages provided by Robertson (1993) in the Darioren area (slice

below the Davras Dag in the NE of the Isparta Cay area), and in the south of Antalya, indicated long-ranging

(Jurasssic–Cretaceous) intervals for the radiolarites, which were then inferred and extended to all the radio-

larite-bearing sequences of the Antalya Nappes. These preliminary datings of the radiolarites provided new oppor-

tunities to describe an elementary series (i.e. including Triassic Halobia beds overlain by Jurassic–Cretaceous

radiolarites), which is tectonically duplicated in several tectonic slices in the Isparta Cay area (Robertson

1993). This work, although pioneering, remained incomplete, with respect to mapping of the area and the chron-

ostratigraphic constraints of this pelagic sequence.

Amongst the microfossils that can be found in the essentially siliceous sedimentary rocks overlying the Triassic

levels, abundant radiolarians are the most useful for biochronostratigraphy. More recent radiolarian work under-

taken by Tekin (1999) and by ourselves provides new and more precise ages.

The aim of this paper is to present the results of new investigations carried out in the area, including extensive

mapping of tectonic slices and the detailed description of two typical successions supported by new and revised

biostratigraphic data (i.e. radiolarians and benthic foraminifera). A comparison with other units in the larger area is

also provided taking into account previous work (Poisson et al. 1984; Poisson 1984; Robertson and Woodcock

1984; Robertson 1993).

2. DESCRIPTION OF THE ISPARTA CAY UNIT

2.1. Internal structure of Isparta Cay unit

In the observed area (Figures 1 and 2) the Isparta Cay unit was thrust onto the Bey Daglar� autochthon during the

Palaeocene. This unit was at first described as a single tectonic unit of the Anatalya Nappes (Gutnic and Poisson

1970). Later, the existence of tectonic duplications was first recognized along the road to Aglasun (Poisson 1977),

284 b. vrielynck et al.

Copyright # 2003 John Wiley & Sons, Ltd. Geol. J. 38: 283–293 (2003)

Figure 1. Outline tectonic map of the Isparta Angle (modified after Gutnic et al. 1979).

tectonics and sediments of antalya nappes 285


then along the stream to Antalya (Robertson 1993). Although these works have shown the tectonic duplication, a

complete mapping was necessary to investigate the complexity of the tectonic setting of the area. The Lower

Miocene ‘neo-autochthon’ covers most of the thrust contacts. As a result an initial thrusting occurred at the time

of the initial emplacement of the Antalya Nappes. However, the presence of small slices of Tertiary sands and marls

intercalated between two slices of the Isparta Cay unit attest an out-of-sequence thrust probably during the Aksu

phase (Late Miocene–Pliocene) (Poisson et al. 2003). Nevertheless, the main slice-thrusting is pre-Miocene.

Figure 2. The Isparta Cay area in southwestern Taurus. The chronology of the main tectonic events, which preceded the closure of the IspartaAngle, are reported (after Poisson et al. 2003).



2.2. Lithostratigraphy

The review of the Isparta Cay Formation in its type locality leads us to map at least ten tectonic repetitions of a

lithologic succession (Figures 2 and 3). In each thrust sheet we recognize the same stratigraphic succession: a marl

and sandstone formation, a carbonate sequence overlain by a radiolaritic formation. They constitute a stratigraphic

unit deposited in a basin and representative of a palaeogeographical entity. Nevertheless, the formations differ

more or less from one slice to another. Several sections have been sampled to determine the age of the two

sequences and to compare this succession with the basinal series, cropping out in other Turkish and Tethyan areas.

The Isparta Cay section

The Isparta Cay section is located along the highway to Antalya, some 20 km from Isparta (Figures 2 and 3, site A;

this section corresponds to unit 6 of Robertson 1993). We observed there a typical section of the basal member of

the Isparta Cay unit. On a sequence of marls and sandstones, we recognize three parts (Figure 4). (1) Micritic lime-

stones are present in 5 to 20 cm thick beds; they also contain calcified radiolarians. Marl interbeds occur through-

out the sequence; they are thin at the base (level a) and reach up to 20 cm in level b. Then, marly interbeds become

thinner (2 cm) again and cherts appear with some ammonites (level c). The beds also become rich in Halobia (level

d and e). In the upper part of micritic limestones, the chert beds are thicker (10 cm); they develop a nodular char-

acter (level f ) where limestones alternate with 5 cm thick cherty beds (level g). (2) The second part of the section

Figure 3. The Isparta Cay unit. General geological map of the tectonic slices and location of the Isparta Cay section (A), Sakarlar section (B),and the section near the bridge along the road to Aglasun which provided good Jurassic radiolarians (C) (for general location see Figure 2).



Figure 4. Detailed logs of the sections of the Isparta Cay: sites A, B and C (see Figures 2 and 3 for site location). The small letters on the left ofcolumns refer to the levels detailed in the text.



shows an alternation of various sediments. On reddish shales (level h) overlain by an alternation of 2 to 5 cm thick

shale beds and 10 cm thick micritic limestone beds (level i) we observe: micritic cherty limestones, alternation of

shales and limestones, a thin layer of green volcanic tuffites, thin-bedded micritic cherty limestones, marls with a

10 cm thick bed of biodetrital calcarenites, micritic limestones with large cherts, Halobia and radiolarians, yellow

to green shales, nodular micritic limestones with brachiopoda and gastropoda and at last micritic limestones with

Halobia and radiolarians. (3) The upper part of the section differs from the former by the lack of Halobia, occur-

rence of microbreccias and appearance of radiolaritic beds. We observed: carbonate conglomerate (level l) and

silicified carbonate microbreccias overlain by radiolarites, shales and thin-bedded nodular limestones (level m).

Then, at the top, occur siliceous calcarenites and cherts or very siliceous radiolarites slumped, with some clastic,

thin-bedded limestones. The section ends with reddish shales, alternating with thin-bedded limestones.

The Sakarlar section (first part)

Sakarlar village is located on a small road, which can be reached from the road going from Isparta to Aglasun

(Figures 2 and 3, site B). The section corresponds to the third tectonic slice overlying the autochthonous Bey

Daglar�. We observe, from the oldest levels to the recent ones, the following succession to the north of the village

(Figure 4). (1) Cherty micritic limestones with thickness of beds ranging between 2 and 30 cm. In some beds

Halobia, radiolarians and, rarely, ammonites occur. (2) Carbonate breccia with compounds of centimetric to deci-

metric size. Some have reefal carbonate facies, but the majority are micritic limestones. (3) Green shales. (4) Car-

bonate breccia which has a lensoidal geometry with extremely variable thickness (1 to 7 m). Elements are graded

bedded from decimetric to centimetric in size. The upper part is silicified. This level contains elements with

Protopeneroplis striata (Weynschenk) known from Aalenian to Kimmeridgian in general, but which is frequent

in the Middle Jurassic of the Taurus platforms. (5) Radiolarites, green in colour.

Compared with the Isparta Cay section, the Sakarlar one differs by the abundance of breccias in place of unit 2

described above and also by the thickness of the micritic beds of unit 1. As a result the Sakarlar deposits seem to

have accumulated in a less deep basinal environment, nearer the slope.

Sakarlar section (second part)

This section is observed in continuity with the previous one (Figures 2 and 3, site B). By houses we leave the road

and, going on the radiolarite beds, we reach the section down in the river where we observe (Figure 4) the follow-

ing: (1) radiolarites, green in colour. The basal beds are of 2–3 cm in thickness; at the top, the beds are 30 cm thick.

In these siliceous deposits we also found beds of siliceous limestones and dolomitic calcarenites. The calcarenites

yield Pseudocyclamina sp., and Trocholina sp.; (2) radiolarites, red in colour; (3) then again, radiolarites, green in

colour.

2.3. Biostratigraphic data

On the basis of a rather rich Halobia fauna, the basal unit of the elementary sequence was attributed to the Late

Triassic (Allasinaz et al. 1974; Poisson 1977; Gutnic et al. 1979). The micritic limestones yielded Halobia: Halo-

bia striatica (Mojsisovics), H. austriaca Mojsisovics, H. charliana Mojsisovics, indicating an Early Norian age, H.

halorica Mojsisovics, H. lineata (Munster), dating Middle Norian. Later, some ammonites are observed in several

sites (Juvatites sp., Clacidites sp., Megaphyllites sp. (det. L. Krystyn)), with some aulacoceratids (Aulacoceras sp.

cf. A. sulcatum), which imply an Early Norian age. So all the basal unit is most probably Norian.

In the upper part of this carbonate member, in the breccias and calcarenites, we observed Protopeneroplis striata

which indicates the Aalenian–Kimmeridgian interval, and above pseudocyclamines and trocholines.

The detailed section of the mainly siliceous upper member has not yet been palaeontologically defined, except in

the calcarenitic turbidites in the Sakarlar section where pseudocyclamines and trocholines are found. However, two

samples of radiolarites cropping out near the bridge on the Isparta Cay along the road to Aglasun (Figures 2 and 3,

site C) have yielded radiolarians.



Sample TO-63 yielded Emiluvia sp., Leugeo hexacubicus (Baumgartner), Parahsuum sp., Paronaella sp. cf.

P. kotura Baumgartner, Podobursa sp., Transhuum maxwelli (Pessagno). L. hexacubicus belongs to and can be

correlated with the Unitary Association Zones (UAZ) 4–8 (Late Bajocian to mid-Callovian/Early Oxfordian:

Baumgartner et al. 1995).

Sample TO-64 yielded Cinguloturris carpatica Dumitrica, Parvicingula (?) spinata (Vinassa), Parvicingula sp.

cf. P. dhimenaensis Baumgartner, Triactoma jonesi (Pessagno). The assemblage characterizes UAZ 7–10, which

correlates with the Bathonian/early Callovian to late Oxfordian/early Kimmeridgian.

Two previous works attempted to date radiolarites forming a part of the Isparta Cay sedimentary sequence. (1)

Three radiolarian assemblages (determined by Pessagno) are provided by Robertson (1993), but only one of them

is important (sample T/83/28) as the fauna is suggestive of a Middle–Late Jurassic age (more precisely, latest Bajo-

cian/early Bathonian to late Oxfordian/early Kimmeridgian, UAZ 5–11 following the recent biozonation by Baum-

gartner et al. 1995). (2) Tekin (1999) extracted two other radiolarian assemblages from radiolarites of the Isparta

Cay series, which he considered as indicative of Middle–Late Jurassic and Early Cretaceous ages (middle Bath-

onian–late Oxfordian and late Valanginian–late Hauterivian). However, based on the species list that he provides

for his Jurassic sample (95-UKT-109) and more particularly the co-occurrence of Linaresia beniderkoulensis and

Paronaella mulleri, its age can be regarded as exclusively Middle Jurassic (middle Bathonian–early Callovian,

UAZ 6–7: Baumgartner et al. 1995).

Our new radiolarian ages and those revised from the available literature, allow us to conclude that radiolarites

accumulated in the Isparta Cay palaeogeographical realm during the late Middle Jurassic (and Late Jurassic ?) and

part of the Early Cretaceous.

As a result, two members constitute the basic sequence of the Isparta Cay unit. Limestones with Halobia are the

major component of the basal member. These carbonate deposits are interbedded with more or less thick marl beds.

The carbonate facies yields Halobia, ammonites and radiolarians, while Aulacoceras was found in the marls.

Palaeontological data give a middle Norian age. In its upper part, this member shows breccias of which the thick-

ness and element size differ from one tectonic slice to the other. Biostratigraphical data indicate a Jurassic age

(Aalenian–Kimmeridgian). The second member is mainly siliceous. Radiolarites are predominant but some cal-

carenite beds occur as reworked clasts of the adjacent carbonate platforms. Radiolarians indicate that their deposi-

tion occurred in late Middle Jurassic time up to, at least, Early Cretaceous. As a result, no Triassic radiolarites have

been identified in the Isparta Cay unit.

The Isparta Cay unit testifies a basinal palaeogeographical entity from Triassic to, at least, Early Cretaceous,

fringed by a carbonate platform of which the border was affected by Early Jurassic tectonics and fed the basin with

calcarenites. The Early Jurassic has not been identified in these sections. It could correspond to the green marls,

which exist in the Sakarlar section, between the Triassic Halobia limestones and the Dogger (Middle Jurassic)

breccias. In other sections, Tekin (1999) reported the existence of a gap corresponding to the Early Jurassic.

3. CORRELATIONS: THE AGE OF RADIOLARITES IN THE ANTALYA NAPPES

In the Antalya Nappes, the radiolarites are present in the basinal sequences and represent the deepest water facies.

Their onset and development in a basin are important to constrain palaeogeographical models. Radiolarites are, in

general, Jurassic and Cretaceous in age, but they can also be Triassic, and they do not always occur in the same type

of sequences. As a result, it is important to review the geological setting of radiolarites in the Anatalya Nappes and

in the neighbouring areas in Turkey.

3.1. Platform margin units (Catal Tepe) and base of slope units (Alakir Cay)

The Catal Tepe unit is considered as a proximal unit adjacent to a carbonate platform of Bey Daglar� type (Poisson

1977, 1984; Poisson et al. 1984; Robertson 1993). This unit is the one in which the stratigraphy is best known from

Late Triassic to Maastrichtian. It crops out along the eastern margin of the Bey Daglar� continuously from the



Tilkideligi Tepe (west of Antalya) to Bilelyeri (20 km farther south). In the Catal Tepe and Tilkideligi sections the

Triassic is represented by marls with reworked blocks of reef limestones and is well dated as early Norian by

ammonites. The origin of these reefal limestone blocks can be inferred by the presence of similar limestones

20 km to the south, in the Bilelyeri area. In the Catal Tepe section the Early Jurassic is represented by red nodular

limestones with Liassic foraminifera (Involutines), in one of the exceptional sections in which the Liassic is iden-

tified (Poisson 1977). In this section the Middle and Late Jurassic are represented by limestone breccias and sands

reworked from a shallow-marine carbonate platform. Some minor intercalations of cherts with radiolarians

occur within the detritic limestones, but true radiolarites are only observed in the Late Cretaceous (Turonian to

Campanian). The Maastrichtian is characterized by calciturbidites and manganiferous marly limestones. As seems

to be the case in the Bilelyeri section, true radiolarites are rather young in the Catal Tepe section. Our Bilelyeri

section (under revision for stratigraphy), is located just to the west of the village and is not one of the Bilelyeri

group sections described by Robertson and Woodcock (1981a). It is relatively reduced in thickness. Its base is

characterized by massive shallow limestones (sometimes with reefs and megalodonts of Triassic age), surrounded

by regularly bedded bioclastic limestones, including reefoid forms looking like Cladocoropsis or similar forms,

and rudists. These beds include cherts and progressively grade upward into radiolarites. As a result, in this section

the radiolarites occurred after the Middle Cretaceous. On the contrary, in the Alakir Cay sections which could be

considered as more distal in the basin, the existence of Jurassic and Cretaceous radiolarites has been reported

(Robertson and Woodcock 1981b), but only Late Jurassic and Early Cretaceous have been formerly identified

in these sections.

As a result, radiolarites occur in the deep basinal depositional environments of the Isparta Cay and analogous

units (i.e. Alak�r Cay) in the Middle–Late Jurassic and the Cretaceous up to the Campanian. In the Catal Tepe units,

which represent the margin of a platform and the slope, the radiolarites are mainly Cretaceous (perhaps mainly

Late Cretaceous: Turonian to Campanian). Radiolarites of Triassic, Early Jurassic and of latest Cretaceous age are

not known to date.

3.2. Other deep water basinal units of the Antalya Nappes

These other units constitute the Godene zone (Robertson and Woodcock 1981c), which could represent the

more distal part of the deep basin. The Godene zone is characterized by Triassic mafic extrusives (pillowed

basalts and massive lava flows) and associated deep-water sediment (Juteau 1970, 1975). New data (Marcoux,

personal communication, 2000) show that the thick succession is a pile of numerous thrust slices of the

same sequence. The basic sequence (under revision) could be a compound of a small number of pillow-basalt

flows. The intercalated sediments include Halobia limestones and, in the Jurassic, radiolarian cherts in some

localities. The predominance of limestones as thin intercalations in the pillow lava indicates that the basin had

not reached very deep water conditions at that time. Other outcrops are known but in rather complicated tec-

tonic contexts, such as to the east of Isparta in the Anamas area and near Kocaaliler between Isparta and Anta-

lya (Robertson 1993). In the absence of direct dating, the age of the radiolarites remains uncertain. In this type

of sequence the Jurassic and Cretaceous deposits, above the volcanics, are rather thin or absent and so the

radiolarites would be reduced.

3.3. The basement of the carbonate platforms

Radiolarian cherts, early Ladinian in age (Tahtal� Dag nappe: Tekin 1999), are included in the Triassic sequences

of carbonate platforms. Radiolarites, attributed to the Triassic, also occur in the Alalkir Cay type nappe in the units

located to the east and southeast of Isparta, but no radiolaria has been found to confirm the age.

As a result, concerning the age of the radiolarites in the Antalya Nappes, we can conclude that they were essen-

tially deposited from the Dogger (Middle Jurassic) to Late Cretaceous (Campanian). They were more frequent in

the period including the Late Jurassic and Early Cretaceous.



4. CONCLUSIONS

In conclusion several points can be underlined.

1. Structures. As previously stated for restricted areas (Poisson 1977; Robertson 1993), the Isparta Cay unit is a

pile of tectonic sheets, which were thrust onto the Bey Daglar� autochthon during the initial emplacement of the

Antalya Nappes in Late Cretaceous–Palaeocene times. About ten tectonic slices have been mapped so far, but

some more may be hidden below the unconformable Lower Miocene deposits. During a later compressional

event (post-Early–Mid Miocene), the initial tectonic pile was affected by new thrusting which made the pile

more complex.

2. Stratigraphy. On the basis of new stratigraphic data the composition of an elementary sequence (first proposed

by Robertson 1993) can be established more properly. Although the elementary successions are not completely

identical from one slice to another, they all include two permanent units: (i) sandstones, marls and Halobia

limestones (Late Triassic); (ii) radiolarian cherts with turbiditic calcarenites, red clays and silts (Jurassic–

Cretaceous). Between these two permanent units another one can be observed from place to place. It is

composed of several breccia beds (coarse-grain in places) and is at least Middle Jurassic in age. In such an

elementary sequence the Early Jurassic has not been characterized, but it could exist between the cherty

Halobia limestones and the green radiolarites. The carbonate breccias are systematically located below the

radiolarites and, as far as they are dated, they are Middle Jurassic in age. They certainly correspond to a tectonic

event, which affected the margin of a carbonate platform at that time. Such events were permanent along the

margin of the Bey Daglar� platform and have been registered all along the Jurassic and Cretaceous (up to

Turonian), in the more proximal unit (Catal Tepe: Poisson 1977). So the Isparta Cay unit corresponds to a more

distal unit in the Pamphylian Basin, probably a base of slope unit.

3. Correlations, age of the radiolarites. At the scale of the Antalya Nappes it appears that the radiolarites are

essentially Jurassic (Middle and Late) and Cretaceous (Early and Late, up to Campanian). The existence of

Triassic radiolarites in units of Isparta Cay type is doubtful if we take into consideration the probable tectonic

duplications, as is the case in the Isparta Cay Unit.

ACKNOWLEDGEMENTS

This work was funded by the CEPAGE (FR32 CNRS) and University Pierre and Marie Curie (Paris VI).

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new insights on the antalya nappes in the apex of the isparta angle: the isparta �ay unit...

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