GEOL. CROAT. ZAGREB 1998 First Evidence of Hercynian Lower Carboniferous Flyschoid Deep-Water Sediments in the Lycian Nappes, Southwestern Turkey He inz W. KOZUR ', Mustafa SENEL' and Kagan TEKIN' Key words: Tavas Nappe, Lycian nappes, Lower Car­ boniferous, Inci rbeleni Fonnation, Deep-water sedi­ ments, Turbidite-olistostrome sequence, Hercyni an orogeny. Abstract For the first time. a deep-water Lower Carbon iferous siliciclastic turbidite-olistostrome unit with many Iydites (partly di sta lly tur­ bid itic) can be dated in the Incirbelcni Fonnation o f the Tavas Nappe (Lyeian nappes) in southwestern Turkey. These nappes belong 10 a ~outhcrn Hercynian Upper Devon ian to Lower Carboniferous nysch Belt that is also known from the Karaburun Zone in western Turkey. A co nodon t fauna, co nsist in g mainly of GnatllOdllS bililleatlls and rcw Lochrica COIII/IIII/a/a without nodose Lochriea species all ows the :Iatin g of chcrl)' limestonc olistoliths as middle to carly late Visean .lgc (V isean 2 10 lower Vi sel.U1 3) . The Lower Carboniferous Hercyn­ ian deep-sea turbidites and olistostromes confirm a northern origin for .he Lycian nappes and a minimum norlh-soulh nappe transport of Ipproximatly 200 km. Nevertheless. the Tavas Nappe originatcd to he so uth of the Izmir- Ankara Zonc because the op hi ol ites of the Izmir - Ankara Zonc fo llow in nappe posi tion above the Tavas Nappe. 1. INTRODUCTION According 10 GOROR el al. (1997) who expressed he prcvailing view, only the Istanbul Block and parts )f the Sakarya Zone in northwestern Turkey had a Her­ ;ynian history. South or the Istanbul block, the Palaco­ ethys is assumed in part s of the Sakarya Zonc, and its Jpper Triassic to Middlc Jurass ic southward directed iubduction is regarded as the reason for the Upper Tri­ Issic opening of Neote th ys wi thin the marginal part of }ondwana (~ENGOR , 1984, 1985). The main Neotelhyan suture zone is assumed in the zmir-Ankara Belt. South or this suture zone, from the (araburul1 Zone in the north to thc BcydagJari Auto­ 'I1thon in thc soulh, the Silurian to Latc Palaeozoic his­ ory was believed to be that of a shallow shelf on the torthcrn part of Gondwana. This view was streng th ­ ned by thc fact that Silurian 10 Permian deep-water edimenl s could not be found or not be dated in th is rca , whereas shallow waleI' deposits of th is age are RczsO u. R3, H-I029 Oudapest . Hungary. Maden Tctkik vc Mallia Gencl MlidlirlligO. Jcotoji EWcHeri Dairesi, E~ki~chir YOIII, 06520 Ankara, Turkcy. known, especially from the Middle Carboniferous to Pemlian, but partly also from the Silurian to Lower Car­ boniferous. This general Palaeozoic development was assumed also for the Tavas Nappe or the Lycian nappes in the study area, where shallow-water, partly lagoonal and continental development continued in the Triass ic (GRAC1ANSKY, 1968, 1972; ERAKMAN et aI., 1982; ~ENEL el aI., 1994). New results since 1995 question the previously gen­ erall y accepted view of the Silurian to Pennian shallow­ water Gondwana shelf dcvelopment that reached north­ wards beyond the Ncotethyan suture zone (Izmir ­ Ankara Belt). KAYA & KOZUR (1995) discovercd for the first lime pelagic conodonts in the Devonian of the Karaburun Zone and KOZUR (J 997a, e , d, in prcss) daled the Karareis " Fonnation" sensu ERDOGAN el al. (1990, 1995) by conodonts, Muellerisphacrida and Radiolaria as Silurian to Early Carboniferous. The rocks can be subdivided according 10 KOZUR (op. eit. ) inlo a Silurian oceanic sequence of shales and Iyditcs and mafi c volcanics, a Late Caledonian Uppe r Silurian to Pragian nysehoid siliciclastic turbidite-olistostrome unit with distal turbidiLic lydites, an Upper Devonian lime­ stone, shale and chert sequence, an Upper Famennian to lower Visean Hercynian turbidite-olistostromc unit , and an upper Visean transitional sequence (rich in ammono­ ids, brachiopods, crinoids, trilobites, conodonts, ostra­ cods, radiolarians) to the molasse type shallow-water Serpukhovian-Bashkirian Alandere Formation. The transitional sequence contains subduction related fel sic to intermediate luffs. Visean rocks of the trans itional sequence werc found al so by CARTDROlT el a l. (1997), They contai n the same ross ils but wcre misiden­ tified as upper Tournaisian , and assumed to be blocks in the "Triass ic" Karareis "Format ion". Thick, very low­ grade metamorphic silici clastic rocks were tentatively assigned without fossil evidence to Ihe Ordovician (KOZUR, 1997a, d). In the Bolkardag Zone, a flyscho id siliciclast ic tur­ bidite-oli stostrome unit wi th dista l turbiditic lydites and fel sic tuffs was reported and assigned to Ihe Early Car­ boniferous by OZCAN et a!. ( 1988). 11 was subsequenl· 1y subdivided and daled by GONCOOGLU & KOZUR (in press) as a Llandovery-Wenloc k deep-sea shale­ chert sequence with turfs, and a Latc Caledonian Upper Silurian to Pragian flyschoid sequence. Thus, the Cale- 16 danian development is identical both in the Karaburun and Bolkardag zones. A Hercynian deep-water sequ­ ence could not be daled in the Bolkardag Unit (not prc­ sent?), where Carboniferous shallow water rocks (main­ ly limestones) are present. DDRR et al. (1995) reported a s imilar , but me tamorphic sequence from the Me n­ deres Massif. According to these authors, an (?)Early Carboniferous flyschoid series overlies black quartzites (? metamorphic lydites) and bas ic volcanics, but this dating is not foss il -proven because of its metamorphic overprint. There fore, a Hercynian deep water develop­ ment can be neith er proven nor excluded in the Men­ deres Mass if. A very interest ing Lower Carboniferous deep water sequence of similar tectonic position to the Tavas Nappe is known from the lower Nohutluk Formation, of the <;:ataloturan Nappe of the Aladag Mountains, at the western end of the Easte rn Taurus Belt. Lower Car­ boniferous radiolarian-rich turbiditic cherty limestones and rare mudstones are overlain by shallow water lime­ stones and sandstones (upper Nohutluk Formation) of middle Visean to Bashkirian age (TEKELI et aI., 1984). The Nohutluk Fomation is unconformably overlain by the shallow water Permian Arka99a Formation which is overlain by variegated shallow water limestones, mud­ stones, marl s and dolomites of Triassic age. The che rty limestone olistoliths in the s ilic ic lastic deep-sea tur­ bidites and radiolarites of the Incirbeleni Formation of the Tavas Nappe are similar to the cherty limestones of the lower Nohutluk Formation that yielded, however, a slightly older Tournaisian - Lower Visean foraminiferal assem blage (TEKELI et aI. , 1984). As these forami ­ ni fe rs are shallow water species, they may have been redeposited in the ca lciturbidites. Alternatively, the upper range of thi s foraminiferal fauna may be Visean 2 . Conodont and radiolarian data from the lower Nohut­ lar Formation are not available. Immediately north of the stable Gondwana, a con­ tinuous SerpUkhovian to Lower Triassic (and younger) deep-water trough was found extending from Crete to western Sicily (KOZUR & KRAHL, 1987; CATA­ LANO et aI., 1991; KOZUR, 1989, 1993) and further to the east in NE Iraq and Oman (BECHENNEC et aI., 1989; VASICEK & KULLMANN, 1988) which should be also present at leas t in SE-Turkey . This southe rn deep-sea trough had, during the Permian, no connection with the Karakaya Zone of NW -Turkey as the Dora­ sham ian radiolarian faunas of Sicily and the Karakaya Complex are totally different (KOZUR, 1993 , 1997b). Moreover, the Karakaya Ocean opened only in the lat­ est Permian (KOZUR & KAY A, 1994 ; KOZUR , 1997b). Opinions concerning a cont inuous Middle Car­ boni ferous to Permian oceanic trough are based on the strat igraphic mis interpretation of red Dorashamian radi ­ olarites as Art inskian to Sakmarian by OKAY & MOS­ TLER (1994), as shown by KOZUR (1997b); the oldest · Pe rmian pelagic sediments (pelag ic limestones) of the Karakaya Zone arc of latest Dzhulfian age (KOZUR & KAYA , 1994). Geologia Croa!ica 5111 Thus, both the presence of Hercynian flysch with Iydites and other deep-water sediments, and (further in the south) the presence of Permian Tethyan deep water sediments should be expected in southern Turkey. Bedded Iydites (black radiolarites) of Late Permian age were reported from the radiolarite-rich, s ilic ic lastic turbidite-olistostrome deep-water sequence of the Incir­ beleni Formation of the Tavas Nappe, at the Ni~angah Tepe locality close to the Yayla Agiliovasi (ERAK­ MAN et aI. , 1982; ~ENEL et aI., 1994; ~ENEL, 1997). These radiolarites and cherty limestone olistoliths from the si liciclastic turbidite-olistostrome of the Incirbeleni Formation were investigated. The deep-water character of this flyschoid sequence could be confirmed . How­ ever, the age of this sequence was proven by conodonts to be Early Carboniferous. 2, LOCATION The investigated section northwest of Te ke pe nin ­ sula (Western Taurides) lies in a rather remote area in SW Turkey between Fethiye and <;:amel i, but east of the road that connects these two towns. The investigated outcrop is SW of the Ni ~angah Hill (Fig. 1). 1000 m W of the sampled outcrop there are a few summer houses for shepherds, and this place is named by the shepherds as the Agiliovasi Yayla. Lydites and cherty limestone olistoliths of a s ilicic lastic turbidite-olistostrome sequ­ ence with many lydites were sampled from the Incirbe­ leni Formation, which had been assigned according to fusulinid faunas from assumed unde r- and overl y ing formations 10 the Murgabian (ERAKMAN et aI., 1982; ~ENEL et aI., 1994), corresponding to the lower-middle Wordian of the international stage subdiv ision. 3, GEOLOGICAL SETTING The Tavas Nappe is the lowermost nappe of the Lycian nappes. It is tectonically underlain by the Ye~il­ barak Nappe which consists of two structural units, the Gbmbe and Yavuz units . The lowe r s tructural unit (Gombe Unit) is represented by Upper Cretaceous lime­ stones (Gebeler Fm. ) and Upper Lutetian-Burdigalian sandstones and shales (Elm ali Fm.). The upper st ructur­ al unit (Yavuz Unit) consists of an uppe r Lutetian to Priabonian fl ysch. The Ye~i1barak Nappe, in turn, rests tectonically on the Beydaglari Autochthon consist ing of the Cretaceous Beydaglari Formation, the Upper Palaeocene-Middle Eocene Di~ ita~tepe Fonnation, and the Lower Miocene Sinek~i Formation. According to ERAKMAN et al. (1982) and ~ENEL et al. (1994), the Tavas Nappe is subdivided into the Karadag Unit of tectonically lower position, tectoni ­ cally overlain by the Tekedere Unit. The Karadag Unit consists of the fo llowing forma ­ tions (from the bottom to the top): Sazak Formation (?Upper Devonian shal es, lime­ stones), r..U l;u r, ,,)cnCI IX I et.:ll1: ! ' Irs ! ~vlacnce 01 11crcyn Ian Lower Cnrboniferous fqyschoid, .. 17 A B MEDITERRANEAN SEA Nisanoih T. 2'\. 1000m * 8 0 7 r:-:-:-l 6 L.:..:..:..:.I _5 g4 ~3 ~2 .' Fi g, I Location map. Rectang les: Positio n of the study area within Turkey (A) and , Illore detailed. wit hin southwestern Turkey (8). Detailed Illap of the locati on in the ri gh!. Legend: J) Karadag Unit consis ti ng in the s tud y area of Kiloluk . Akkavak. Sar i ta~. Karapi nar and BeJcnkavak formations: 2) Tckedere Unit eonsisl ing of <;atakdere. Incirbelcni and Nit'<1.ngahtcpe formations; horizonlally hatched area: Main occurrence of bedded chel'l s and some limestone oii stoiith s, narrow stripe in the NE are iimeslO ncs; 3) <;cnger Fonnution; 4) Aga<; li Forma· tion; 5) Serpentinite (Marmaris ophiolite nappe); 6) Pliocene <;ameJi Formation (lacustrine depos its); 7) Quaternary; 8) Sampling poi nt. Kiloluk Formation (M idd le Carbon iferous bioclastic limestones, dolomites, dolomitic limestones), Akkavak Formation (Lower Permian crystalline lime­ stones, dolomites, shales), Sarita~ Formation (?Upper Anisian to Lower Ladinian sands tones), Karapinar Formation (Ladinian black limestone), Belenkavak Formation (Carnian-Norian sandstones, siltstones, shales). The Tekedere Unit is thrust over the Karadag Unit. The thrust boundary is sti ll preserved in the southwest­ ern corner of the study area (Fig. I), but often masked by later block fau lting (e.g., in the western part of the investi gated area, where the block with the Karadag Unit is relatively elevated (+) against the Tekedere Unit (-) , as shown in Fig. I). Acco rding to ~ENEL et al. (1994) and ~ENEL ( 1997), the Tekedere Unit consists of the following for­ mations (from the bottom to the top): (:atakdere Formation (crystalline limestones), Incirbeleni Formation (shales, sandstones, limestone " lenses", Iydites, volcanics) , and the Ni§angahtepc Formation (dolomites, limestones). The <;atakdere Formation contains, according to ~ENEL ( 1997), the following fossils (algae and Forami­ nifers): Mizzia velebitana (SCHUB ERT), Globivalvl/li­ na vanderschmitti REICHEL, Hemigordius rellzii REI­ C HEL, Neosehwagerina aatiel/Ii/era SCHUBERT, Pachyph/oia sp., Staffel/a sp., and Neo/l/sl/lina sp. The Ni§angahtepe Fonnation contains the followin g fo ssils: Mtzzia velebitano (SCHUBERT) , Colalliel/a sp., Geinitzina sp. , Globivalvulina /vaeca REICHEL, Hemigordius renzii REICHEL, Neoschwagerina sp .• and Paehyph/oio sp. (~ENEL, 1997). Both formations were assigned to the Murgabian (= Lower-M iddle Wor­ dian). They were deposited in a shallow shelf environ­ ment. The Incirbeleni Fonnation was assumed to be si tua­ ted in normal stratigraphic order between these two for­ mat ions (~ENEL et aI. , 1994). As it has not yie lded any fossi ls , thi s formation was also ass igned to the Mur­ gab ian (ERAKMAN et aI. , 1982; ~ENEL et aI. , 1994; ~ENEL, 1997). ~ENEL ( 1997) did not exclude a Car­ boniferous age. Thi s, however, wou ld excl ude a posi­ tion of the Incirbeleni Formation between the <;atakdere and Ni§angahtepe formations. The placement of the Incirbeleni Fonnation between two stable carbonate plat form success ions of the same age was not logical for sedimentological-facial reasons. The Incirbeleni Formation is composed of mafi c vol- 18 canies, pa rtl y pillow lavas, overlain by shales, bedded Iyditcs and clast ics of turbiditic character (graded sha­ les, siltstones, sandstones, in the upper pari also micro­ conglomerates and quartzi lic sandstones). Moreover, it also contains limestone olistoli ths. This sequence does not fit into a co ntemporaneous carbonate platform sequence. Our d iscovery of Lower Carboniferous conodonts in the Inc irbc le ni Formation definite ly excludes it from the ass um ed sequence <;atakdere Formation - lnc irbc­ lcni Format ion - Ni§angahtcpe Formation. There arc two possible ex planat ions for the present juxtaposi tion: ( I) The Inc irbe lcni Format ion on one s ide and the Gatak­ clerc Formati on & Ni~angahtepe Formation on the other s ide be long to d iffe re nt units, tectonically juxtaposed to each o the r. (2) The <;;atakdere Formation and the Ni§an­ gahtepe Formation are parts of the o ri ginal cover beds of the deep-sea Inc irbeleni Formati on that was late r partly tectonica ll y s liced into thesc carbonate platform rocks. The tecton ic emplacement of the Incirbe leni Forma­ tion is a lso ind icated by the fact that it is accompanied by an adjaccnt me lange zone. This zone contains be ige q uart zites, Iydites, reddish radiola rites and red lim e­ stones with volcan ics. We have not yet inves tigated the age or these rocks. Afte r a lengthy hiatus, the Rhaetian to lowe r Liassic Ge nge I' Formation Iran sg ress ively ove rlies diffe re nt o lder units of the Tavas Nappe. The <;enge r Formation cons is ts o f a bauxite layer, reddi sh cong lome rates, sandstones and s ilts tones (MONOD e t aI. , 1983 . It is fo ll owed by the Liass ic Aga~ l i Format ion (dolomites and algal limestones) and the upper Toarc ian to Maas­ trichtian Babadag Form ation (chert y limes tones, at the base uppe r Toarc ian ammon iti co rosso). Afte r an unconformity, the re is an Upper Palaeocene to Lower Miocene flysch wi th some alka li basalts. We could not find in the fi e ld ev idence that the (engel' Formation is scaling an Early C immerian overthrust of the Tekedcre Unit on the Karadag Uni t. The tec tonicall y h igher nappes of the Lycian nappe system (Bodrull1 Nappe, Dumanlidag Nappe, Mannaris Ophiolite Nappe, Giilbahar Nappe, and Domuzdag Nap­ pe in ascending orde r) are in the study area on ly repre­ sented by serpentinites of the Marmaris Ophiolite Nap­ pe (Fig. I). The Pliocene Gamel i Fo rmation cove rs d iffe re nt units o f the T avas Nappe and the Marmari s Ophi o lite Nappe. It consis ts of lacustrine deposits. 4. RESULTS On ly the Ine irbe le ni Formation was inves ti ga ted , both the chert y limestone olistoliths and the Iyd ites. The conodo nt fauna o f the cherty limestone o li sto lith s is ri ch in spec imens but consists only of two de tenninable spec ies presented by the diagnostic Pa elements and by the other c lements of the apparatus. The faun a is dom iw nated by GlIOlllOdus bilinealus (ROUNDY) (PI. I , Figs. Geo logia CrO:l l iCfl 51/ 1 1-3), whe reas Lochriea commllfafa (B RA NSON & MEHL) (PI. J, Fig. 4) is rare . MEISC HNER ( 1970) rec­ ognized that such a fauna occurs in the middle Visean (V 2 and lower V 3). Be low this level, G. biliuealus is not present. Both species range up to the lower Namuri ­ an. However, in the upper Visean (upper V 3) and low­ er Namurian (Serpukhovian) , they are accompanied by Lochriea species that displaces nodes or ri bs on the cup o f the Pa eleme nt, such as L. crLlCljormis (CLA RKE), L. 11I01101l0dosa (R HODES , AUSTIN & DRUCE), L. I1IUllillodosa (WIRTH), L. l1Io llocoSlalO (PAZUKHIN & NEMIROVS KA Y A) , L. 1I0doso (B ISC HOFF), L. sellckellbergica NEMIROVSKA Y A, PERRET & MEI­ SC I-lNER, and L. zieg leri NEM IRO VSKAYA, PER­ RET & MEISCHNER (e.g. MEJSC HNER , 1970; HIG­ GINS, 1974; HIGGINS & WAGNER-GENTIS, 1982; RILEY, 1993; SKOMPSKI e t a I. , 1995). Moreover, in th is level , also different subspecies of GJ/{Jfhoc/us g irlyi /-l ASS occur , such as G . girly i girly i HASS, G. girlyi col/il1sol1i RHODES , A USTIN & DRUCE, G. girlyi ill lerlll edius GLOBENSKY , G gir lyi rhodesi HIG­ G INS, G. girly i simplex DUNN, and G. girfyi sOl/iae RHODES, AUSTIN & DR UCE (HIGG INS , 1975). None of these species were fou nd in the limestone olis toliths of the Incirbeleni Formation. The absence of G. girfy i m ay be caused by the g reat wate r d ep th or prov incialism, because this species is also not present in the very rich upper Visean deep-wate r conodont faunas o r the Karaburun Peninsula, but Lochriea species with sculptu red cup are ve ry common in the uppe r Visean of the Karaburun pe ninsula (KOZU R, 1997a , e, d). The re­ fore , a middle Visean (V 2 and early V 3) age for the limes tone olistol iths is ind icated. The Iyd itcs arc very rich in radiola rians, but unfo r­ tunate ly , they could not be di ssolved from the rocks. Conodonts are rare in the Iydites and are only represen t­ ed by indeterminable broke n forms . An exact age deter~ mination is impossible for radiolarians that are enclosed in the rock. However, there we re no rccogn ized form s charac te ristic for beds younger th an Ea rl y Carbonife r­ ous. O lde r ages can be ne ither exc luded nor provcn for a part of the lydites. S. CONCLUSIONS I. The sequence of the Inc irbe leni Formation of (he Tavas Nappe (Lycian nappes) is the sOllthernmost dis­ covered Hercynian oceanic to suboceanic seque nce in Turkey. It consis ts of mafic volcanics and pillow lavas, overl ain by sha les and bedded radiolarites (ma in ly Iydi tes), de posited be low the CCD, overlai n by s ili ci­ c lastic turbid ites, o li stoslromes, turbid iti c sandstones, grcywaekes and mierocongiome rates. 2. The southernmost prev iously known occurre nce of Hercyni an deep~wa t e r sequcnces th a t e nded in the uppermost Early Carboniferous, and we re mostly over­ lain by Serpukhovian to Middle Carboni fe rous shallow­ wate r deposits (by this a Pal aeo tethyan o rig in can be l\.ozur, .")CIlCI &: I CKm: 1 ' l r~ 1 I:Vl(lcnce 0 1 t lercyn lan L ower C" rtlOnirerou ~ Flyschoid ... 19 exc luded ), is in the Karaburun Zone (KOZUR, 1997a, c) . The Incirbeleni Formati on is litholog ically ve ry similar to the Hercynian sili c iclastic turbidite-oli s­ tostrome unit of the Karaburun Zone. 11 may originally have bee n a part o f this zone, De ri vatio n from areas o rig ina ll y to the south is not poss ible because the re a Gondwana shallow-wate r she lf was present in Hercyn­ ian time, Thi s proves a northe rn ori g in for the Lyc ian nappes, and requ ires a minimum no rth-south nappe tran sport of about 200 km. The Lower Carbonife rous Hercy ni an deep-sea turbidit cs and oli stostromes con ­ finn a northern origin of the Lycian nappes and a mini­ mum no rth-south nappe transport o f about 200 km. However, the T avas Nappe originated somewhat south of the Izmir - Ankara Zone because the ophiolites of the Izmir -A nkara Zone follow in nappe position immedi ­ ate ly above the Tavas Nappe. The lower Nohutlllk Fo rm ation of thc C;atalo!uran Nappe in the Aladag Mountains probably represcnts the outc r she lf-s lope of the southe rn Hercyni an ocean , at the transiton to the Lower Carbon iferous Peri gondwana carbonate platform. 3. The olistoliths o f cherty limestones contain a con­ odont fauna of Visean 2 - Lower Visean 3. The bedded Iydites havc a radiolarian fauna not younger than Earl y Carbonife rous, As most of the thicke r bedded cherts (mostly lydites) are not ye t dated , a pre-Carbon iferous age ca nno t be excluded for parts of the deep-wate r sequcnce. 4. Probab le overlying beds (un investigated) of the Tekede re Unit consis t of molasse type c rinoidal lime­ stones, sandstones, vol canics, volcanic conglomerates that were probably originally overlain by platform car­ bonates with Middle Permian (Guadalupian) fusulinid s « atakdere and Ni §angahtepe fomlations), S, If the cora ls o f the Sazak Formation of the Karadag Unit are correctly de termined and give a late Dev oni an age , as so far assumed (e .g. ~ENEL, 1997), then the Tavas Nappe would consis t o f two basicall y diffe rent nappes, one for the Karadag Unit with a typi ­ ~al Devonian -Carboniferous shallow-water Gondwana she lf deve lopment , and a sccond nappe with the Her­ :::ynian deep-wate r developmelll , overlain by a molasse lype and carbonat e p lat form shallow water deve lop­ me nt o f (?)Midd le Carbon ife rou s to Middle Permi an Ige. Acknowledgements The inves ti gatio ns by H,W. KOZUR were carri ed lut in the fram e of a NATO C P grant (TUbitak). Prof. =. GONCUOGLU , Ankara, discussed many problems md gave a good introducti on to the Pal aeozoic his tory )f Turkey. Prof. Dr. A. RAMOYS , Ljubljana, and Prof. Jr. H. MOSTLER , Inn sbruek, improved the pape r by 'ery care ful rev iewing . Many thanks are extended fo r his fin anc ial and scientific support. 6. REFERENCES BECHENNEC, F., LE M ETOUR, 1., RABU, D. , BEU­ RRIER, M. , BOURDlLLON DE GRISSAC, e. , DE WEYER , 1', BEURR1ER, M. & YILLEY , M. (1989): The Hawashina Nappes : stratigraphy, paleo­ geography and structural evolution of a fragment of the south-Te thyan passive continental margin, - In: ROBERTSON, A.H.F., SEAR LE, M.P. & RIES , e. A. (cds.): The geology and tectonics of the Oman region, Special Publications of the Geologica l Soci­ e ty of London , 49, 21 3-223, London. CARIDROIT, M , DEGARDIN, 1.M. , DERYCKE, e. , LETHIERS , F., MARCOUX, F. , MILT-IAU , B., PILLEYU IT, A. & Y ACHARD, D. 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KOZUR , H. & KAYA, O. (1994): First evidence of pelagic Late Permian conodont s from NW Turkey.­ N. Jb. Geol. Paliionl. Mh. , 1994/6, 339-347 . KOZUR , H. & KRAHL, J. ( 1987): Erster Nach weis von Radiolarien im tethyalen Perm Europas.- N. Jb. Gcol. Pal'ont. , Abh., 174/3,357-372. MEISCHNER, D. (1 970): Conodonten-Chronologie des deutsehen Karbons.- e.R. Congr. Intern. Stra l. Gool. Carbonif. , Sheffield 1967, 1169- 1 180, Shef­ field. MONOD, 0 ., ME~HUR, M. , MARTIN, M. & LYS, M. (1983) : Decouverte de Dipneustes Triasiqucs (Cera­ todontiformes, Dipnoi) dans Ie formation de <;:enger (Arkoses ROllges) du Taurus Lycien (Turquie occ i­ dentale).- Geobios, 16/2 , 161 -168. OKAY , A.I. & MOSTLER, H. ( 1994): Carboniferous and Permian radio larite blocks from the Karakaya Com plex in northwest Turkey. - Tr. J. Earth Sc i­ ences, 3, 23-28 , Ankara. OZCAN, A., GONCOOGLU, M.e., TURHAN, N., UYSA L, ~. , ~ENTORK, K. & I~IK , A. (1988): Late Paleozoic evolution of the Kiihtahya-Bolkardag Belt. - METU Journ . Pure App l. Sci. , 2 1/1 -3, 21 1- 220, Ankara. RILEY, N.J . (1993): Dinantian (Lower Carboniferous) biostratigraphy and chronostratigraphy in the British Isles .- Journ . Geo l. Soc. London , 150, 427-446, Belfast. ~ENEL, M. (1 997): I: 100000 ol<;ekli, Tii rkiye jeoloji haritalari serisi , no. 2 : Fe lhiye - LS.- Paftas i, An­ kara, 30 p. ~ENEL, M. , AKDEN IZ, N., OZTORK, E. M., OZDE­ MIR, T. , KADINKIZ, G. , METlN, Y., OCAL, H. , SERDAROGLU, M. & OR<;:EN, S. (1 994): Fethiye (Mugla) - Kalkan (Antalya) ve kuzeyinin jeolojisi.­ MTA Rep. No. 976 1 (Unpublishcd). ~ENGOR , A.M.e. ( 1984): The Cimmeride orogenic system and the tectonics of Euras ia .- Geo!. Soc. Amer. , Spec. Paper, 195,82 p. ~ENGOR , A.M.e. (1985) : Die Alpiden lind die Kim ­ meriden: Die verdoppelte Geschichte der Tethys .­ Geol. Rundsch. , 74, 181-2 13. SKOMPSKI, S., ALEKSEEV, A. , MEISCHNER, D., NEMIROVSKA Y A, T., PERR ET, M.F. & V ARK­ ER, W.J . ( 1995): Conodont distribution across the .H""'''' " ... " .... , u<. , .... '"'' • L..r'l.1 L.. l 21 PLATE I The fi gured material is housed in the Geological Institute of the Innsbruck University. All figured specimens are from sample 96/640, middl e Vi sean cherty limestone o listolith w ithin the Incirbe leni Formati on SW of the Ni ~angah Hill at Agiliovasi Yayla, SW Turkey. 1-3 Gllarhod"s bifilleollls (ROUNDY); Fig. I : upper view, x 50, rep.-no. 23297/IlI- 19; Fig. 2: obli que lateral­ upper view, x 100, rep.-no 23297/1IT-24; Fig. 3: upper view of a specimen with broken free blade, x 80 , rep.­ no. 23297/111-20. 4 Lochriea commlllora (BRANSON & MEHL), upper view, x 100, rep.-no. 23297/111-2 1. 5 Glla/hod"s sp. , upper view of a juvenile specimen, x 200, rep.-no. 23297/1II-22. 22 Visean/Namurian boundary.- COUf. Forsch.-Inst. Scckcnberg, 188, 177-209. TEKEU, 0., AKSA Y, A., DRGDN, B.M. & 1~IK, A. (1984): Geology of the Aladag Mountains.- In: TEKEU, O. & GONCDOGLU, M.e. (eds.): Geolo­ gy of the Taurlls Bell, 143-158, Ankara. Geologia Croalica 51/1 VASICEK, Z. & KULLMANN, J. (1988): Eine Ammo­ noidecn Fauna von Sosio-Typ (Guadalupian , Ober­ perm) aus Kurdistan (Iraq).- Palaeonlograph ica, A, 204/1-3,95-115. Manuscript received December 1,1997. Revised manuscript accepted May 18, 1998.