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Early Ludlovian (early Late Silurian) palynomorphs from the Pala-eozoic of Çamda¤, NW Anatolia, Turkey

Çamda¤ Paleozoyi¤inde Erken Ludloviyen (erken Geç Siluriyen)palinomorflar›, KB Anadolu

Iskra LAKOVABulgarian Academy of Sciences, Geological Institute, Acad. G. Bonchev St., Bl. 24, 1113 Sofia,BULGARIA

M. Cemal GÖNCÜO⁄LUMiddle East Technical University, Department of Geological Engineering, 06531 Ankara, TURKEY

ABSTRACT

In the Çamda¤ area in north-western Anatolia, newly discovered tectonic slices including the Shale-Siltstone Mem-ber of the F›nd›kl› formation yielded a diverse palynological association with determinable acanthomorphic acri-tarchs and prasinophyte algae and tabular structures. From these, the short-ranging species Ammonidium ludlo-wense, Eisenackidium wenlockium, Gorgonisphaeridium listeri listeri and G. succinum are of biostratigraphical in-terest as they are restricted to the early Ludlow. This is so far the first early Late Silurian palynological data fromNW Turkey and suggests that the deposition in the Çamda¤ area was more proximal, compared with the correla-tive units in the Perigondwanan ‹stanbul and Balkan Terranes.

Key Words: Çamda¤, early Late Silurian, NW Turkey, paeleogeography, palynomorphs.

ÖZET

KB Anadolu’da Çamda¤ yöresinde yeni saptanan bir tektonik dilimde yüzeylenen F›nd›kl› formasyonuna ait fieyl-Silttafl› Üyesi tan›mlanabilir özellikteki akantomorfik akritarklar, prasinofit algler ve yass› yap›lardan oluflmufl zen-gin bir palinolojik topluluk içermektedir. Bunlardan Ammonidium ludlowense, Eisenackidium wenlockium, Gorgo-nisphaeridium listeri listeri ve Gorgonisphaeridium succinum gibi türler k›sa konakl› olduklar›ndan biyostratigrafikaç›dan önemlidirler ve erken Ludloviyen yafl›na iflaret ederler. Bu bulgu, KB Anadolu’daki ilk erken Geç Siluriyenpalinolojik bulgusudur ve bu dönemde Çamda¤ alan›n›n Perigondwana kökenli ‹stanbul ve Balkan tektonik birlik-lerine göre k›taya daha yak›n konumda oldu¤unu gösterir.

Anahtar Kelimeler: Çamda¤, erken Geç Siluriyen, KB Anadolu, paleoco¤rafya, palinomorf.

Yerbilimleri (Earth Sciences), 26 (1), 61-73Hacettepe Üniversitesi Yerbilimleri Uygulama ve Araflt›rma Merkezi DergisiJournal of the Earth Sciences Application and Research Centre of Hacettepe University

M.C. Göncüo¤luE-mail: [email protected]

INTRODUCTION

The Paleozoic of NW Anatolia between ‹stanbuland Cide (Figure 1) along the Black Sea coastis incorporated to the “‹stanbul Nappe” of fien-gör and Y›lmaz (1981) or “‹stanbul Zone” ofOkay (1989). The Paleozoic formations in this

unit are classically known as the “Paleozoic of‹stanbul” and considered previously as part ofthe eastern European “Hercynian chain”. Basedon stratigraphic dissimilarities it had beenshown recently (Göncüo¤lu et al., 1997; Göncü-

o¤lu, 1997; Göncüo¤lu and Kozur, 1998, 1999)that the “‹stanbul Nappe” actually includes twodifferent terranes: “‹stanbul Terrane s.s.” in thewest and the “Zonguldak Terrane” in the east(see Figure 1). The Çamda¤ “Massif” (Kipman,1974) geographically located between them, re-mained as a problematic area. In the previousstudies it was univocally accepted that the Çam-da¤ area was a “paleo-high” through most of theOrdovician and Silurian (Kaya, 1988; Önalan,1982; Ayd›n et al., 1987; Derman and Tuna,2000), as no Silurian rocks were identified inthis region. Recent studies (Kozlu et al., 2002;Gedik and Önalan, 2002; Göncüo¤lu and Sac-hanski, 2003), however, have shown that thethick succession of low-grade metamorphicblack shales with minor black siltstone and li-mestone interlayers (Yayla Formation of Kip-man, 1974, or F›nd›kl› formation of Yazman andÇoku¤rafl, 1984) is in fact of Silurian age.

The F›nd›kl› formation includes numerous thrustsheets. Based on a correlation between thesetectonic units, Kozlu et al. (2002) differentiatedfrom bottom to the top three informal units: theBlack Shale Member, Shale-Siltstone Memberand the Shale-Limestone Member. The upperpart of the Black Shale Member yielded Upper

Llandoverian (Telychian) graptolites, whereasthe “Orthoceras Limestone” interlayers in theupper part of the Shale-Limestone Member wasdated as Pridoli.

In this study, the authors present their first earlyLate Silurian fossil findings from the Shale-Silts-tone Member of the F›nd›kl› formation and revi-se the stratigraphy of the Silurian succession inthe Çamda¤ area. The early Ludlovian (earlyLate Silurian) palynomorph data reported in thisstudy are so far the first findings in NW Anatoliaand have important constraints on the paleoge-ography and the depositional environment ofthe middle Silurian in this region. Finally, the Si-lurian stratigraphy of the Çamda¤ area is beingcorrelated with the neighboring areas in Turkeyand with those of tectonic units in the easternBalkan Peninsula in order to evaluate its pale-ogeographic position in regard with the Gond-wanan/Peri-Gonwanan terranes.

GEOLOGY AND STRATIGRAPHY

The Çamda¤ “Massif” is located between thetowns Hendek and Karasu to the NE of Adapa-zar› and covers an area of approximately 400km2 (see Figure 1). The Paleozoic rocks in

62 Yerbilimleri (Earth Sciences)

KASTAMONU

Devrekani

Safranbolu

ZONGULDAK

Amasra

Mengen

BOLU

ADAPAZARI

‹ZM‹T‹STANBUL

B L A C K S E A

TEK‹RDA⁄

MARMARA SEA

‹znik Lake

BULGARIA

0 100 km

Çamda¤

Sünnüce Da¤›

N

Basementcomplex ‹stanbul terraneZonguldak terrane Undefined

Kaplandede D.

Hendek

Almac•k D.

ANKARA

BLACK SEA

Study Area

‹ZM‹RANTALYA

Figure 1. Distribution of the Paleozoic rock units in the ‹stanbul and Zonguldak terranes in NW Anatolia and thelocation of the Çamda¤ area.

fiekil 1. KB Anadolu’da ‹stanbul ve Zonguldak birliklerinde Alt Paleozoyik kayalar›n›n da¤›l›m› ve Çamda¤ alan›-n›n konumu.

Çamda¤ are highly deformed and slightly meta-morphosed. The lower part of the Paleozoicsuccession is mainly represented by variegatedarkoses, quartz-sandstones, siltstones andmudstones (So¤uksu, Kocatöngel, Bakacak,Kurtköy and Aydos formations in Ayd›n et al.,1987; Gedik and Önalan, 2002) that cover thesouthern part of the massif. Except a single pte-rineid pelecypod finding with a wide age range(Gedik and Önalan, 2002) no fossil findings hadbeen reported from these units in the Çamda¤area and the suggested Ordovician age in theprevious work is mainly based on the correlati-ons with the better-dated units in ‹stanbul andZonguldak areas. The contact to the overlyingF›nd›kl› formation is generally faulted.

The F›nd›kl› formation crops out mainly in thecentral and northern parts of the massif within aroughly E-W trending anticline, dissected by nu-merous south-verging thrust-faults. The revisedcolumnar section of the Ordovician to Devonianrocks in the Çamda¤ area with a brief descripti-on of the rock-units is given in Figures 2 and 3.F›nd›kl› formation in its upper part displays agradational transition to the overlying Lower De-vonian B›çk› Member of the Kartal Formation.

The studied part of the Silurian rocks is locatedbetween Mollahasan Tepe and Karadere Villa-ge on the Hendek-Karaali road in the centralpart of Çamda¤ (see Figure 2). The studied sec-tion starts at a thrust-fault at the Süngüt road-junction where recrystallized, thick-bedded De-vonian limestones (limestone member of theKartal Formation) juxtapose the violet-red-gray,silica-cemented slates with sandstone interla-yers that resemble the Ordovician Bakacak For-mation. Along the road-section, F›nd›kl› formati-on rests with a thrust-contact on the BakacakFormation and the Kartal and Aydos formationsare not represented. The studied section termi-nates in the north at the contact between F›n-d›kl› and Kartal formations to the south of Kara-dere Village.

The lower part of the F›nd›kl› formation was in-formally named as the Black Shale Member ofthe F›nd›kl› formation by Kozlu et al. (2002). It ismainly composed of a thick and monotonoussuccession of gray to greenish gray, well-cle-aved shales with minor black siltstone and limyshale interlayers. Very thin-bedded black shales

alternating with gray and brownish siltstones inthe lower 10th m of the member include Spirog-raptus spiralis (Geinitz), Spirograptus falx (Su-ess), Monoclimacis vomerina (Nicholson), Mo-nograptus priodon (Bronn), Monograptus parap-riodon Boucek, Monograptus (Globosograptus)mancki Hemmann, Monograptus curvus Manck,Diversograptus ramosus Manck, Retiolites an-gustidens Elles and Wood, Cyrtograptus (Bar-randeograptus) pulchellus Tullberg, indicativefor the spiralis Zone of the Late Llandovery,Telychian (Göncüo¤lu and Sachanski, 2003).

The overlying Shale Siltstone Member displaysa gradational contact to the Black Shale mem-ber and is characterized by alternations of darkgray-greenish black siltstones and shales withdark green-black, pyrite-bearing limy siltstones.In contrast to the siltstones of the underlyingBlack Shale Member, the siltstones here are

Lokava and Göncüo¤lu 63

Karadere Mah.

to Karaali

EXPLANATIONS

to Süngüt

to Hendek

Küçükyayla T.

Ademtarla T.

Mollahasan T.

N

1

Formationboundary

Kabalak Mb.

Lmst Mb.

B›çk› Mb.

F›nd›kl› Fm.

Bakacak Fm.

Kar

tal F

m.

CD-19

CD-20

SettlementRoad

Creek

Samples withpalynomorphs

Reverse fault

Thrust fault

Samples withgraptolites

Orthoceraslimestone

Mollahasan D

.

CD-16-17

CD-22

0 2 km

Figure 2. Geological map of the study area.fiekil 2. Çal›flma alan›n›n jeoloji haritas›.

very rich in mica detritus. The shales are finelylaminated and include tiny flakes of sericite. Thesiltstones display grading and lamination andinclude sub-rounded clasts of feldspar and qu-artz next to coarser-grained detritial white mica.The individual limy siltstone bands are up to 4 mthick and massive. From several samples takenfrom the Shale-Siltstone Member only onesample (CD-19, Figure 2) yielded more or lesspreserved indicative fossils of middle Silurianage, as presented in the next chapter.

The siltstones and shales of the Shale-SiltstoneMember grade upward into black shales with li-mestone and dolomitic limestone interlayers ofthe Shale-Limestone Member. The limestonesof the member are dark gray to brown in color,and very rich in up to 30 cm long orthocone cep-halopods, crinoids and brachiopods and can be

used as marker horizons to decipher the verycomplex folding and faulting. They include Pri-dolian conodonts (Kozlu et al., 2002).

PALYNOLOGICAL FINDINGS AND THEIRIMPLICATIONS

Pilot samples have been taken from all threemembers of the F›nd›kl› Formation. Amongthem, five samples (CD- 16, CD-17, CD-19, CD-20 and CD-22) yielded organic-walled microfos-sils. The samples have been processed usingthe standard palynological technique by soluti-on with HCl and HF. As a whole, the palynologi-cal material is scarce, dark, opaque, coalified,flattened and hardly determinable, sometimesas silhouette forms. After lightening using HNO3during 60 minutes, acritarchs available in samp-le CD-19 have become transparent and deter-minable.


Figure 3. Generalized columnar section of the Ordovician to Lower Devonian rocks in the Çamda¤ area.fiekil 3. Çamda¤ alan›nda Ordoviziyen-Alt Devoniyen istiflerinin genellefltirilmifl stratigrafik dikme kesidi.

Black Shale Member

The samples CD-16 and CD-17 are taken fromthe Black Shale Member, which was recentlydated on graptolites as Telychian by Göncüo¤-lu and Sachanski (2003). The palynological as-sociation is very poor and mainly consists of co-alified opaque acantomorthic acritarchs andthree species of tubular structures of AnteturmaTrichomoformis Bugress and Edwards (1991):Laevitubulus tenuis Burgess and Edwards, L.crassus Burgess and Edwards and Porcatitubu-lus strupus Wellman. These species were previ-ously reported from Upper Llandovery to Loch-kovian continental deposits in the British Isles(Wellman, 1995), as well as from Pridoli to Em-sian marine shales from the Moesian Terrane inBulgaria (Lakova, 2001).

Shale-Siltstone Member

The samples CD-19 and CD-20 are taken fromthe Shale Siltstone Member whose age was notdetermined on fossils till now. The palynological

association of the sample CD-19 is diverse interms of organic-walled microfossil groups: opa-que trilete spores (Plate 1 Figures 1, 13, 17 and18), single cryptospores - spore dyads (Plate 1Figure 5) and tetrads (Plate 1 Figure 6), chit ino-zoans (Plate 1 Figure 14), scolecodonts (Plate1 Figure 16), ?mazuelloids (Plate 1 Figure 19),as well as determinable acanthomorphic acri-tarchs and prasinophyte algae and tubularstructures. The following acritarch and prasi-nophytes species occur in CD-19 sample:

Ammonidium ludloviense LISTER, 1970(DORNING, 1981) (Plate 1 Figure 11)Cymatiosphaera sp. cf. C. octoplanaDOWNIE, 1959 (Plate 1 Figure 3)Comaspheridium brevispinosum (LIS-TER, 1970) MULLINS, 2001 (Plate 1Figure 4)C. williereae (DEFLANDRE andDEFLANDRE-RIGAUD, 1965) SAR-JEANT and STANCLIFFE, 1994Eisenackidium wenlokense DORNING,1981Gorgonisphaeridium listeri listeriMULLINS, 2001 (Plate 1 Figure 8)


Series

StageTaxa

Ammonidium ludloviense

Cymatiosphaera octaplana

Comasphaeridium brevispinosum

Comasphaeridium williereae

Eisenacidium wenlockense

Gorgonisphaeridium succinum

Gorgonisphaeridium listeri listeri

Oppilatala ramusculosa

Veryhachium trispinosum

Llan

dove

ry

Wen

lock

Ludl

ow

Prid

oli

Low

erD

evon

ian

Gor

stia

n

Figure 4. Known ranges of the acritarch and prasinophyte taxa recorded from the Shale Siltstone Member in Cam-da¤ area. (Sources: Lister, 1970; Dorning, 1981; Le Herisse, 1989; Molyneuxet al., 1996; Mullins, 2001).

fiekil 4. Çamda¤ alan›nda F›nd›kl› formasyonunun fieyl-Silttafl› Üyesinden al›nan CD-19 nolu örne¤in akritark veprasinofit türlerinden baz›lar›n›n stratigrafik konaklar› (Kaynaklar: Lister, 1970; Dorning, 1981; Le Heris-se, 1989; Molyneuxet al., 1996; Mullins, 2001).

Gorgonisphaeridium succinum LISTER,1970 (Plate 1 Figure 12)Lophosphaeridium sp. indet.Oppilatala ramusculosa (DEFLANDRE,1945) DORNING, 1981 (Plate 1 Figure 2)Verychachium trispinosum (EISENACK,1938) STOCKMANS and WILLIERE,1962.

The tubular structures in sample CD-19 are rep-resented by four species: Constrictitubulus cris-tatus (Plate 1 Figure 15), Porcatitubulus annula-tus (Plate 1 Figure 7), Porcatitubulus strupusand Ornatifilum granulam, all four previously re-ported from Upper Llandovery to Emsian conti-nental and marine succession from England,Wales, Scottland, Ireland, Sweden, Norway,USA, Bulgaria (see Wellman, 1995; Lakova,2001). The sample CD-20 is much poorer in or-ganic-walled microfossils - only single opaquesilhouettes of spores and acanthomorphic acri-tarchs and two species of tubular structures: L.tenuis, and L. crassus.

Shale Limestone Member

The age of this member is Pridoli on conodontsand nautiloids (Kozlu et al., 2002). The palyno-logical record of sample CD-22 from this mem-ber is very scarce, consisting of only single in-determinable chitinozoans resembling the ge-nus Calpichitina, as well as the tubular speciesL. crassus (Plate 1 Figure 13).

All acritarchs and prasinoppyte species recor-ded from the Shale Siltstone Member occur inthe Silurian worldwide. A. ludloviense, E. wen-lockium, G. listeri listeri and G. succinum are ofbiostratigraphical interest as these are short-ranging species restricted to the Wenlock andLudlow in England, Sweden and Ukraine (Dor-ning, 1981; Le Herisse, 1989; Molyneux et al.,1996; Mullins, 2001).

The species C. brevispinosum, E. wenlockenseand G. succinum start their ranges at the baseof the Upper Wenlock - Sheinwoodian Stage.On the other hand, A. ludloviense, E. wenloc-kense and G. listeri listeri are not known abovethe Gorstian Stage (the Lower Ludlow) (Figure4). It should be mentioned that E. wenlockenseand G. listeri listeri which are of very short stra-tigraphical occurrence were recorded only in theWelsh Borderland in England (Dorning, 1981;

Mullins, 2001) and it is possible these are nottheir complete ranges.

As a whole, the acritarch and prasinophyte as-sociation recorded in the Çamda¤ area (sampleCD-19) is of early Late Silurian age and of widegeographical distribution over three paleoconti-nents - Avalonia, Baltica and Gondwana. Seve-ral species, such as C. octoplana, C. brevispi-nosum, C. williereae, O. ramusculosa and V.trispinosum were reported from England, Ire-land, Belgium, France, Sweden, Norway, Ukra-ine, Austria, USA, Canada, Argentina, Spain,Libya and Saudi Arabia (Le Herisse, 1989; Mul-lins, 2001). The acritarch association from theShale-Siltstone Member contains some indicati-ve species suggesting early Ludlovian age. Theranges of these species, as well as the scarcityof specimens do not allow a more fine and pre-cise age determination.

Along with the marine microphytoplankton (acri-tarchs and prasinophytes), there is a relativelycommon record of land plant microfossils suchas trilete spores and cryptospores and tubularstructures. Despite the identified tubular structu-re species are too longer-ranging forms to be ofbiostratigraphic use, the occurrence of allocht-honous land plant elements clearly indicatesthat a more or less constant fluvial terrestrial se-diment input existed in the Çamda¤ area duringmid-Silurian time.

CORRELATION WITH OTHER SILURIANROCK-UNITS IN NEIGHBORING TERRANES(NW TURKEY, TAURIDES AND THEBALKAN MOUNTAIN)

The detailed stratigraphy of the middle Silurianrocks in NW Anatolia is only known in the ‹stan-bul (Yalç›nlar, 1956; Haas, 1968; Kaya, 1988)and Safranbolu (Dean et al., 1997; 2000) areas(see Figure 1). To the east of ‹stanbul (Gebzearea, see Figure 1) the early Late Ludloviansuccession is mainly characterized by the “Akvi-ran Serie” of Haas (1968) which corresponds tothe “Halysites-Limestone” of Peackelmann(1938). The “Tavflan Tepe Schichten” in the lo-wermost part of the Akviran conformably overli-es the variegated clastics of the Upper Ordovi-cian and is composed of greenish marls thatgrade into “flaser-limestones” by increasing limecontents. The brachiopods and conodonts


(Walliser, 1964) from this succession indicate aWenlockian age. The following “BaglarbasiSchichten” mainly includes sandy limestoneswith Pentamerides of Wenlockian. Upward fol-lows reddish crinoidal limestones with corals ofWenlockian-Late Ludlovian age. The confor-mably overlying “Cakillidere Schichten” of the“Akviran Serie” is made up of gray, irregularlybedded, fine-grained limestones with conodontsand has been ascribed to the siluricus- Biozone(Ludlovian) of Walliser (1964). They are follo-wed by stromatopora and tabulata-rich, irregu-larly bedded limestones (“Untere Pelitli Schich-ten” belonging to the latialatus and crispus zo-nes of Ludlovian) that grade into nodular limes-tones (Obere Pelitli Schichten of crispa andeosteinhornensis biozones of Walliser (1964)and hence the Ludlovian-Pridoli boundary ac-cording to the recent stratigraphic nomenclatu-re). There is an overall agreement between theprevious researchers (Haas,1968; Kaya,1973,1988; and Önalan, 1982) that the Wenloc-kian-Ludlovian part of the succession in ‹stanbularea is represented by reef-type carbonate de-position. Starting with the deposition of flaserand nodular limestones of Early Pridoli age atransition to basin-type deposition is suggested.

The Paleozoic succession in the Karadere-Zirzearea (Safranbolu, Figure 1) in the Zonguldakterrane was studied by Arpat et al. (1978) andDean et al. (1997, 2000). In this area, the F›n-d›kl› formation in its lower part includes black si-liceous shales with graptolites of middle Llando-very (Aeronian) age and acritarchs (Dixellopha-sis remota (Deunff), Tylotopalla sp. and Very-hachium europaeum Stockmans and WIllIére).Following a lack of exposures of about 80 m,gray, schistose mudstones monograptid grapto-lite-bearing shales with Monograptus flemingii(Salter) and Pristiograptus cf. parvus (Ulst) we-re reported. This part of the succession did notyield acritarchs but the graptolites are indicativefor the upper part of the Wenlock series. Theblack shales are unconformably overlain by De-vonian conglomerates and carbonates, so thatthe “Orthoceras Limestones” found in the Çam-da¤ were not encountered in this succession.

Compared with the ‹stanbul and Safranbolu are-as, there are still fragmentary data on the Siluri-an rock-units in the Çamda¤ area. However, thenew data (Göncüo¤lu et al, 2003) indicate that

almost the entire Silurian may be represented indifferent tectonic slices of the F›nd›kl› Formati-on. The depositional environment of the Silurianrocks in Çamda¤ differs from the ‹stanbul area,where reef-type carbonate deposition domina-tes.

In the Taurides in southern Turkey, Silurianrocks rest with a parallel unconformity on the la-te Ordovician glacier-related sediments (Göncü-o¤lu and Kozlu, 2000; Ghienne et al., 2001).The overlying Puflcu Tepe Shale formation iscomposed of thinly bedded, laminated black tolight-gray fissile shales. The lower part is silice-ous with fine bands of shales, whereas the up-per part is carbonaceous with bands of blacklydites. In its lower part it includes thin layers ofgray “Orthoceras Limestones” that yielded co-nodonts of middle Llandovery to latest Llando-very - earliest Wenlock age (Göncüo¤lu et al.2004). In the Central Taurides, in Konya area,dark colored siltstones and shales alternatingwith tuffaceous layers and distal turbiditic blackcherts (ribbon cherts) within the low-grade me-tamorphic Turbidite Unit (Göncüo¤lu et al.,2000) yielded Muellerispherida of Wenlock age(Kozur, 1999). The middle and upper parts ofthe Silurian in the Taurides is represented bythe Yukar› Yayla and Karatafl formations (De-mirtafll›, 1984; Dean and Monod, 1990). It istransitional to the underlying Puflcu Tepe Shaleformation and consists of alternations of blackshale and dark gray limestone. The limestone atthe bottom is medium-bedded, brown to dark-gray, wavy bedded, coarsely nodular and rich innautiloids. The middle part of the formation ischaracterized by black, thin-bedded shales withconcretions containing brachiopods and trilobi-tes. The upper member consists of an alternati-on of black shales and dark-gray limestonesand is conformably overlain by Devonian shelf-type limestones.

Late Early Silurian acritarchs were reported yetonly from south-eastern Turkey (Dadafl Forma-tion around Diyarbak›r) by Erkmen and Bozda-¤an (1979) and Steemans et al. (1996). The as-semblage from Dadas Formation is youngerand differs in species from that of Çamda¤ areain north-western Turkey. In Bulgaria, sedimen-tary rocks of Wenlock to Pridoli age occur in twoareas - in the Moesian Terrane (Moesian Plane,north Bulgaria) and in the western part of Bal-


kan Terrane (the core of Svoge anticline to thenorth of Sofia).In the Moesian Terrane, only twoboreholes penetrated Wenlock and Ludlow de-posits, both in the NE Bulgaria (Yanev, 1992,1998). In R-2 Vetrino well, the Landovery to Pri-doli is represented by ca. 1200 m thick sequen-ce - between depths of 1500-2700 m, of mainlyblack and gray shales, calcareous shales andsome marls and limestones (Spasov and Ya-nev, 1966), Llandovery age being proved on co-nodonts. In OP-2 Michalich well, the Llandoveryto Pridoli represents a more than 500 m thickseries - between depths of 3200-3761 m, of mo-notonous black shales and siltstones (Lakovaand Yanev, 1989; Lakova, 1992). The Wenlockand Pridoli were dated on chitinozoans. In wes-tern part of the Moesian Terran, in R-1 Dalgo-deltsi well, Pridoli series is represented by lessthan 80 m uniform black shales dated on chiti-nozoans (Lakova, 1985).

In the Balkan Terrane, the Wenlock and LudlowSeries are represented by the black graptoloticshales of the Mala Reka Formation (90 m thick)and the laminated siltstones of Yabukov DolFormation (ca. 230 m thick), the stratigraphicage being based on rich graptolitic faunas (Sac-hanski and Tenchov, 1993; Sachanski, 1998).

When compared to the Çamda¤ succession,the Silurian in the Balkan Terrane is similar incertain extent, as it consists of black shales ofWenlockian and Gorstian age covered by lami-nated slates of Ludfordian and Pridoli age, withonly single limestone lenses with Scyphocrini-tes and bivalves. On the contrary, the Siluriansuccession of the Moesian Terrane is rather dif-ferent, as it is represented mainly by black sha-les and black to gray siltstones of much greaterthickness and without graptolites.

CONCLUSIONS

A early Late Ludlovian microphytoplankton dis-covered in the middle part (Shale-SiltstoneMember) of the F›nd›kl› formation in Çamda¤(Adapazar›, NW Anatolia) contains some orga-nic-walled microfossil groups: opaque triletespores, single cryptospores - spore dyads andtetrads, chitinozoans, scolecodonts, ?mazuello-ids, as well as determinable acanthomorphicacritarchs and prasinophyte algae (Ammonidi-um ludloviense, Cymatiosphaera sp. cf. C. oc-

toplana, Comasphaeridium brevispinosum, C.williereae, Eisenackidium wenlokense, Gorgo-nisphaeridium listeri listeri, Gorgonisphaeridiumsuccinum, Lophosphaeridium sp. indet., O p p i -latala ramusculosa, Verychachium trispinosum)and tabular structures (Constrictitubulus crista-tus, Porcatitubulus annulatus, Porcatitubulusstrupus and Ornatifilum granulatum). This asso-ciation contains some indicative species sug-gesting early Late Ludlovian age and is so farthe first palynomorph data from NW Anatolia.

The lithologies and the organic-walled microfos-sils of the Shale-Siltstone Member suggest thatit was deposited in an anoxic shallow-marineenvironment with clastic sediments supply froma fluvial source, rich in white mica. The rock-units of the same age in ‹stanbul and Tauridebasins are significantly different and suggest arelatively deeper depositional environment.Consequently the Çamda¤ area was probablylocated nearshore at this period. In the Zongul-dak basin, there is a stratigraphic gap betweenthe graptolite-bearing upper Wenlock seriesand the unconformably overlying Emsian shal-low-marine carbonates, being the characteristicfeature of the Zonguldak terrane. A far-distancecorrelation with the middle Silurian deposits inBulgaria suggests that the studied successionin the Çamda¤ area is similar to the Balkan Ter-rane rather than the Moesian one.

Acknowledgments

This study is funded by the bilateral project BAS- TUBITAK (102Y157) “Correlation of PalaeozicTerranes in Bulgaria and NW Turkey in the fra-mework of tectono-palaeogeographical evoluti-on of Gondwana”. It is also a part of Project NZ-813 financed by the Bulgarian National Scienti-fic Council. Dr. N. Bozdo¤an and Dr. Aral ‹.Okay are gratefully acknowledged for theirconstructive review.

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PLATE 1/ LEVHA 1

Diverse palynomorphs from the mid-Silurian of Çamda¤ Section. (All figures from sample CD-19, x700, except sta-ted otherwise).Çamda¤ kesidindeki Orta Siluriyen kayalar›ndaki palinomorflar. (Tüm görüntüler CD-19 nolu örnektendir. Baflkaflekilde belirtilmemiflse büyütme x700 dür).

1. Trilete spore (trilet spor).2. Oppilatala ramusculosa (Deflandre, 1945) DornIng, 19813. Cymatiosphaera sp. cf. C. octoplana DownIe, 19594. Comasphaeridium brevispinosum (LIster, 1970) MullIns, 20015. Spore dyade.6. Spinate spore tetrade.7. Fragment of Porcatitubulus annulatus Burgess and Edwards,19918. Gorgonisphaeridium listeri listeri MullIns, 20019. ? Land plant fragment (Karasal bitki parças›), x440.10. Trilete spore (trilet spor).11. Ammonidium ludloviense LIster ,1970 ex DornIng, 1981.12. Gorgonispharidium succinum LIster, 197013. Laevitubulus crassus Burgess and Edwards, 1991, CD-22, x700.14. Calpichitina sp. indet.15. Constrictitubulus cristatus Burgess and Edwards,1991.16. Scolecodont.17, 18. Indeterminable trilete spores (tan›mlanamayan trilet spor).19. ?Mazuelloid.



PLATE 1/LEVHA 1

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