palynostratigraphic, palaeovegetational and palaeoclimatic...

Palynostratigraphic, Palaeovegetational and PalaeoclimaticInvestigations on the Miocene Deposits in Central

Anatolia (Çorum Region and Sivas Basin)

M‹NE SEZGÜL KAYSER‹ & FUNDA AKGÜN

Department of Geological Engineering, Dokuz Eylül University, T›naztepe Campus, Buca,TR–35160 ‹zmir, Turkey (E–mail: [email protected])

Abstract: Palynostratigraphy of the Neogene coal-bearing sediments in the Çorum region and Sivas Basin has beendetermined, and three sporomorph associations have been defined. Sporomorph association A is described fromthe Samsun-Havza region and is of latest Burdigalian age. Sporomorph association B is described from the Çorumregion and Sivas Basin and is of early–middle Serravalian age. Sporomorph association C is described from theSivas-Vas›ltepe region and is of earliest Tortonian age. Sporomorph association A indicates warm subtropicalclimatic conditions and the Coexistence Approach (CA) results are: mean annual temperature (MAT) 19 °C, meanannual coldest month (CMT) 9.75 °C, mean annual warmest month (WMT) 27.2 °C, mean annual precipitation(MAP) 1217–1322 mm, and a mean annual temperature range of (MART) 17.45 °C. Sporomorph association Bcharacterizes a subtropical climatic condition, and the CA results indicate similar temperatures to those of the latestBurdigalian period. For the early–middle Serravalian age, the MAT values range between 18 and 19.15 °C, theCMT values are between (-0.8)–10.6 °C, and the WMT between 24.7–27.7 °C, respectively. Generally the MAPsof the latest Burdigalian and early–middle Serravalian times are high. The range of the MART values relate to thepalaeovegetation and palaeotopography during early–middle Serravalian time, during which increases of the MARTvalues from the Çorum region indicate high palaeotopographic conditions. Sporomorph association C indicates awarm-temperate climate and the CA results are: MAT 19 °C, CMT 9.4 °C, WMT 27.7 °C, MAP 1187–1574 mm,and MART 18.3 °C. Palaeovegetation of the Çorum region and Sivas Basin characterizes a lacustrine environmentsurrounded by mountains from the latest Early to Middle Miocene. Open vegetation areas were widespread inearliest Tortonian time, and thus different from the palaeovegetation of the latest Early to Middle Miocene period.

Key Words: Miocene, palynology, palaeovegetation, palaeoclimatology, Çorum region, Sivas Basin

Orta Anadolu’nun Miyosen Tortullar›nda Palinostratigrafik, Palaeovejetasyonalve Palaeoiklimsel Araflt›rmalar (Çorum Bölgesi ve Sivas Havzas›)

Özet: Çorum bölgesi ve Sivas Havzas›’n›n Neojen yafll› kömür içerikli tortullar›n›n, palinostratigrafisi belirlenmifl veüç sporomorf toplulu¤u tan›mlanm›flt›r. Sporomorf toplulu¤u A, Samsun-Havza bölgesinde tan›mlanm›flt›r ve engeç Burdigaliyen yafll›d›r. Sporomorf toplulu¤u B, Çorum bölgesi ve Sivas Havzas›’ndan tan›mlanm›flt›r veerken–orta Serravaliyen yafll›d›r. Sporomorf toplulu¤u C, Sivas-Vas›ltepe bölgesinden tan›mlanm›flt›r ve en erkenTortoniyen yafll›d›r. Sporomorf toplulu¤u A, ›l›k subtropikal iklim koflullar›n› yans›tmaktad›r ve ‘CoexistanceApproach’ analizi (CA) sonuçlar› s›ras›yla; y›ll›k ortalama s›cakl›k (YOS) 19 °C, en so¤uk ay›n s›cakl›¤› 9.75 °C(ESoA), en s›cak ay›n s›cakl›¤› 27.2 °C (ESA), y›ll›k ortalama ya¤›fl miktar› 1217–1322 mm (YOY) ve y›ll›k ortalamas›cakl›k amplitüdü (YSA) 17.45 °C dir. Sporomorf toplulu¤u B, subtropikal iklim koflullar›n› karakterize eder ve busporomorf toplulu¤a ait CA sonuçlar›, en geç Burdigaliyen dönemine ait CA sonuçlar›yla benzerdir. Erken–ortaSerravaliyen dönemi için, YOS de¤erleri 18–19.15 °C aras›nda de¤iflmektedir. S›ras›yla ESoA de¤erleri (-0.8)–10.6°C aras›nda ve ESA de¤erleri 24.7–27.7 °C dir. Genellikle en geç Burdigaliyen ve erken–orta Serravaliyen dönemineait YOY de¤erleri yüksektir. Erken–orta Serravaliyen döneminde, YSA de¤erleri paleovejetasyon vepalaeotopo¤rafyaya ba¤l› olarak de¤iflmektedir ve bu dönem boyunca, Çorum bölgesine ait örneklerin YSAde¤erlerindeki art›fl, yüksek palaeotopografik koflular› gösterir. Sporomorf toplulu¤u C, ›l›man iklim koflullar›n›yans›tmaktad›r ve CA sonuçlar› s›ras›yla YOS 19 °C, ESoA 9.4 °C, ESA 27.7 °C, YOY 1187–1574 mm ve YSA 18.3°C’dir. Erken–orta Serravaliyen döneminde Çorum bölgesi ve Sivas Havzas›’n›n paleovejetasyonu, da¤lar ile çevriligölsel ortam› karakterize eder. En geç Erken ve Orta Miyosen periyodundaki palaeovejetasyondan farkl› olarak, enerken Tortoniyen döneminde aç›k alanlar daha genifl alanda yay›l›m göstermektedir.

Anahtar Sözcükler: Miyosen, palinostratigrafi, paleoiklim, palaeovejetasyon, Çorum bölgesi, Sivas Havzas›

Turkish Journal of Earth Sciences (Turkish J. Earth Sci.), Vol. 17, 2008, pp. 361–403. Copyright ©TÜB‹TAKFirst published online 27 December 2007

361

MIOCENE PALAEOCLIMATOLOGY IN CENTRAL ANATOLIA

362

Introduction

The Çankırı Basin, one of the main sedimentary basins incentral Anatolia, is composed of mainly ophiolitic rocks ofthe Neo-Tethyan suture zone (Figure 1). The basin wascreated by the closure of the Neo-Tethyan Ocean betweenthe Sakarya Continent and Kırflehir Block in Cretaceous toEocene times (fiengör & Yılmaz 1981; Tüysüz 1993;Erdo¤an et al. 1996). The Çankırı Basin, in which thickdetrital sedimentary sequences and volcanic rocks of theEocene age were deposited, developed between theKırflehir and Sakarya continents. These sediments wereunconformably overlain by evaporate-bearing Miocenecontinental successions (Tüysüz 1993; Erdo¤an et al.1996). The Çorum region is located in the eastern part ofthe Çankırı Basin.

The Sivas Basin is another important central Anatolianbasin, and is located north of the Kırflehir Massif (Figure1). The sedimentary sequence is relatively simple with asuccession of marine and continental formation: deepmarine Upper Cretaceous to Eocene clastic rocks (withlocal volcanic intercalations), and Upper Eocene andOligocene red continental clastic rocks with evaporites,unconformably overlain by Oligocene and Early Mioceneshallow marine limestones and marls. Late Miocene andPliocene terrestrial facies include continental clastics andlacustrine limestone (Poisson et al. 1996; Özden et al.1998).

Many geological and palaeontological studies (Birgili etal. 1975; Tekkaya et al. 1975; Ünay & fien 1976;Özdemir & Pekmezci 1983; Erdo¤an et al. 1996; Poissonet al. 1996; Toprak 1996; Özden et al. 1998; Rückert-Ülkümen 1998; Akgün et al. 2000a, b, 2002; Özdemir2000; Türkmen & Kerey 2000; Atalay 2001) have beenmade for different purposes in these study regions. Moststudies were in the Neogene sediments of the ÇankırıBasin. These studies stated that coal bearing sediments ofthis basin were Oligo–Miocene deposits, although detailedstudies on the age of widespread coal-bearing sedimentsof the Çorum region have not been done. The overallobjectives of the present study are to: (1) define thepalynostratigraphy of coal-bearing sediments in theMiocene deposits of the Çorum and Gemerek regions, (2)reconstruct the palaeovegetation in the Early, Middle andearliest Late Miocene surroundings of the Sivas andÇorum regions (central Anatolia) based on high-resolution pollen analysis of the coal samples usingbotanical taxonomy and quantitative approach to pollen

data, (3) infer palaeoclimatic conditions of the study areasand to correlate with the numerical climatic results ofthese regions, (4) discuss palaeoclimatic effects onpalaeovegetation and (5) to compare the palaeoclimaticresults with recent climatic properties.

Geological Setting

Palaeontology in the Çankırı-Çandır region was firststudied by Tekkaya et al. (1975) and Ünay & fien (1976)in the region west of our study area. These authorsstated that coal-bearing sediments of the Çandır regionwere of Middle and early Late Miocene age based on themammalian fossils (Figure 2). Rükert-Ülkümen (1998)studied the fish beds of Alpagut-Dodurga near Çorum,which have decisive importance for the entire LateOligocene–Middle Miocene sedimentation in the Çankırı-Çorum Basin. Toprak (1996) studied chemical analyses,XRD, SEM, spectral emission fluorescence measurements,palynology, rock and organic petrographical analyses inthe Dodurga formation of Evlik, Kargı, ‹ncesu, ‹kizler,Ayva, Dodurga and Kumbaba coal horizons (Çorum-Osmancık). Palynological data from these coal horizonsshow that the Dodurga formation sporomorphassociation is of Middle Miocene age. Kaymakcı et al.(2001) studied the stratigraphy and palaeontology in theÇankırı-Çandır Basin, in which the mammalian data, andcoal-bearing sediments indicate an Early–Middle Mioceneage. Numerous authors have discussed the stratigraphyand palaeontology of the Sivas Basin (Poisson et al. 1996;Özdemir 2000; Türkmen & Kerey 2000; Sümengen et al.1990; Burijin & Saraç 1991; Özden et al. 1998; Akgün etal. 2000a; Langereis et al. 1990). Sümengen et al.(1990) studied rodent fauna of the Kayseri-Sivas Basin(Yeniköy; Harami1, 3; Horlak 1a, b, 2; Gemerek;Kaleköy; Karaözü; Dendil and ‹¤deli) ranging in age fromMiddle Oligocene to Early Pliocene, with a gap in theEarly Miocene. Langereis et al. (1990) studied themagnetostratigraphy in the Kayseri-Sivas Basin inAnatolia, and found that the magnetostratigraphy of theGemerek section, plus the age constraint of 14.9±0.7Ma, yields several possible correlations on the basis of theimplied sedimentation rates and the lithology of thesection. A correlation yields an age of 16.4 Ma for theGemerek mammal fauna, which is at present preferred(Figure 2). Our study areas are located in the Çorumregion (to the north of the Çankırı Basin) and theGemerek region in the Sivas Basin (Figure 1).

M.S. KAYSER‹ & F. AKGÜN

363

C

KIRŞEHİR

MASSIF

SİVAS

RHODOPE

Rhodope-Pontide

reverse or thrust fault

Figure 1. Major continents and suture zones of central Anatolia and locations of the sedimentary basin developed along collision zonebetween these belts (modified from Tüysüz 1993; Poisson et al. 1996).

The Çorum Region

Basement rocks in the Çorum region include Mesozoiclimestone, gneiss, micaschist and basal conglomerate. TheEocene sediments unconformably overlie the basementrocks (Seymen 1981; Tüysüz 1993; Erdo¤an et al.1996). The Eocene succession, which is the main part ofthe basin fill, is unconformably overlain by theLower–Middle Miocene continental deposits (fien et al.1998). The Kızılırmak and Bozkır formations composedof terrestrial conglomerates, laminated shales andevaporate, are distinguished in the Middle Miocenedeposits. Both of the formations are laterally andvertically passed (Birgili et al. 1975; Erdo¤an et al. 1996;Akgün et al. 2002a). This succession in turn is overlainwith angular unconformity by alluvial deposits ofPleistocene age (Figures 3 & 4).

The Gemerek Region

Basement rocks include Palaeozoic peridotite, gneiss,schist, amphibolite, quartzite and marble. ThePaleocene–Eocene sediments, comprising limestone,conglomerate and sandstone, overlie the basementunconformably. The Oligocene rocks, consisting ofsandstone, claystone and gypsum alternations,unconformably overlie the Paleocene–Eocene succession.The Yeniçubuk formation, which was deposited in the

Middle–Late Miocene, unconformably overlies theOligocene rocks (Özdemir 2000; Türkmen & Kerey2000), and is composed of terrestrial sandstone,siltstone, marl, limestone and lignite intercalation in itslower part. The upper part of this formation is composedof interbedded limestone, basalt and pyroclastic rocks.The overlying Upper Miocene–Pliocene E¤erci formationconsists of marl, siltstone, claystone, sandstone,conglomerate, and is overlain with angular unconformityby alluvial deposits of Pleistocene age (Figures 3 & 4).

Material and Method

Using the following techniques, a total of 61 samples ofthe Kızılırmak formation (Çorum region) and theYeniçubuk formation (Sivas-Gemerek region) wereprepared for quantitative counting. All the samples wereprocessed following the standard palynologicalprocedures, which include treatments with HCl, HF, andHNO3.

Defining palynofloras of the Çorum and Gemerekregions were applied using the ‘Coexistence Approach’(CA) proposed by Mosbrugger & Utescher (1997). Thus,palaeoclimatic reconstructions of all fossil floras arederived from the CA. The CA is based on the assumptionthat the climatic requirements of Tertiary plant taxa aresimilar to those of their nearest living relatives (NLRs).


364

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The climatic ranges in which a maximum number of NLRsof given fossil flora can coexist are called coexistenceintervals (Bruch & Gabrielyan 2002). The palynofloras ofsamples in the Çorum and Sivas-Gemerek have beenanalysed with respect to five climatic parameters: meanannual temperature (MAT), mean temperature of thecoldest month (CMT), mean temperature of the warmestmonth (WMT), mean annual precipitation (MAP) andmean annual range of temperature (MART). Usually the

resolution and the reliability of the resulting coexistenceintervals increase with the number of taxa included in theanalysis. The resolution of the calculated climatic intervalsvaries with respect to the parameter examined; it is thehighest for temperature related parameters (MAT, CMTand WMT) where it is commonly in the range of 1–2 °C(Mosbrugger & Utescher 1997; Bruch & Gabrielyan2001; Pross et al. 2001).

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Figure 3. (A) Simplified Geological Map of the Çorum region (modified from Tüysüz 1993) and Sivas Basin (modified from Özdemir2000). (B) Geological Map of the Sivas-Gemerek area (modified from Özdemir 2000).


366

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As an additional climate proxy, we have definedsporomorph assemblages of the Çorum and Gemerekregions by the relative proportion of palaeotropical (P)and arctotertiary (A) elements. According to classicaldefinitions (e.g., Mai 1991; Planderová 1991; Nagy1992, 1999), the arctotertiary elements are used for theplants which grew in cold areas during the Palaeogene ina temperate to warm temperate climate andcorrespondingly occur today in the temperate zone(Ivanov et al. 2002). In contrast, palaeotropic elementsare plants, which have their present distribution primarilyin the tropics (Ivanov et al. 2002).

The use of multivariate analytical methods inpalynological and palaeobotanical studies has becomemore widespread (Spicer & Hill 1979; Kovach 1988,1989). The choice of methods depends on the type ofdata and the specific problems being solved (Kovach1989). Detrended correspondence analysis has beenchosen for this study in order to identify groups ofpalaeocommunity types and samples that are associationsof the variables contained within the data available usingthe MVSP (version 3.1).

Palynological Associations

In this study, sixty-one palynological samples taken fromthe Kızılırmak formation of the Samsun-Havza, Çorum-Evlik, ‹kizler, Kumbaba, Dodurga, Ayva, Amasya-Çomuareas (in the Çorum region) and the Yeniçubuk formationof the Sivas-Karagöl, Akalın and Vasıltepe areas (in theGemerek region) were examined (Figure 4). Only thirtyof these samples were counted as the other samplescontained too few spore and pollen species for statisticalevaluations. Eight spores, 17 gymnosperms, 41angiosperms, 2 algae, fungal spores and an incertae sedisspecies were identified in this study (Plates I–VIII). Therelative percentages of plant taxa are given in apalynological diagram (Figure 6). The relative abundanceof sporomorphs was considered, classifying more than15% as highly abundant; 5% to 14% as abundant; 1%to 4% as sparse; less than 1% as rare and “*” as veryrare or sporadic. The presences of the three sporomorphassociations have been recognized on the basis ofquantitative and qualitative contents of sporomorphs.

Sporomorph association A of the Kızılırmak formationis recognized in samples from the Samsun-Havza area,which includes abundant and varied sporomorph

elements. Samples of the Samsun-Havza lignites contain adistinctly high abundance of P. microalatus (Pinus(haploxylon-type)), averaging 7% and observed in almostall the samples. In some samples Polypodiaceae, Quercus(henrici-type) (10%), Quercus and Ulmus are abundant,(5.5–14%), whereas Podocarpus, Cathaya, Taxodiaceae,Cupressaceae, Sparganiaceae, Myricaceae, Engelhardtia,Carya, Salix, Castaneae, Cyrillaceae, Nyssa and Sapotaceaeare sparse (1%–4%). Schizaceae, Sphagnaceae,Selaginella, Osmundaceae, Poaceae, Lemnaceae,Nymphaeaceae, Juglandaceae, Pterocarya, Simarubaceaeand Cycadaceae are rare (1–>1%). Pinus (silvestris-type),Corylus, Tilia, Onagraceae, Myrtaceae, Reevesia, Alnus,Carpinus, Fagaceae and Chenopodiceae are sporadicallyrepresented in these samples. Algal forms of Pediastrumsp. and Botryococcus braunii are present in samples fromthe Samsun-Havza lignites (Figure 5, Plate I).

Sporomorph association B was detected in theKızılırmak formation in the Çorum-Evlik, Ayva, Zambal,‹kizler, Kumbaba, Dodurga, ‹ncesu and Alıcık areas andthe Yeniçubuk formation in the Sivas-Karagöl and Akalınareas. This sporomorph association includes a highabundance of Polypodiaceae, Ulmus and Pinus(Haploxylon-type) (15–43%). In some samples,Castaneae, Cyrillaceae, Oleaceae, Poaceae, Carya,Engelhardtia, Quercus and Cupressaceae are abundant(5–14%). Osmundaceae, Picea, Pinus, Podacarpus,Simaraubaceae, Taxodiaceae, Nymphaeaceae, Cycadaceae,Alnus, Quercus (T. henrici), Salix, Nyssa, Oleaceae,Myricaceae, Carpinus, Pterocarya, Poaceae andSparganiaceae are present sporadically in sporomorphassociation B (1–4%). Schizaceae, Sphagnaceae, Pinus(silvestris-type), Abies, Sequoia, Arecaceae, Corylus,Juglandaceae, Tilia, Reevesia, Fagaceae, Araliaceae,Sapotaceae, Chenopodiaceae, Lemnaceae, Lonicera,Ephedraceae, Symplocos, Onagraceae, Umbelliferae andRhus are rare and sporadically represented, withpercentages between 1% and <1%. Algal forms ofPediastrum sp. and Botryococcus braunii are only presentin samples from the Çorum-Evlik, Zambal, ‹skilip, ‹ncesuand Alıcık lignites (Figure 5). The speciesRhamnaceaepollenites triquetrus, Lonicerapollis cf.gallwitzi, Iteapollis angustiporatus, Juglanspollenitesverus, Reevesiapollis triangulus and Rhuspollenitesornatus are recorded in this study but have not beenmentioned in the Turkish Miocene previously (Figure 5,Plates II–VII).


367

Sporomorph association C was recognized in theYeniçubuk formation (Sivas-Vasıltepe region). Thisassociation is characterized by high abundances of Pinus(haploxylon-type) and Poaceae (>15%). In some samplesPolypodiaceae, Pinus (silvestris-type), Taxodiaceae,Nymphaeaceae, Myricaceae, Ulmus, Quercus, Cyrillaceaeand Chenopodiaceae are abundant (5–14%), whereasEngelhardtia, Juglandaceae, Platycarya, Carya, Salix,Quercus (henrici-type), Fagaceae, Castaneae, Oleaceae,Asteraceae (Tubulifloreae-type), Cycadaceae andUmbelliferae are scarce (1–4%). In samples from theselignites, Gleichenia, Sphagnaceae, Podacarpus,Cupressaceae, Sequoia, Ephedraceae, Sparganiaceae,Tilia, Alnus, Reevesia, Nyssa, Cichorieae (Liguliflorae-type), Tricolporopollenites sp. (geranium-type) andSapotaceae are observed rarely and sporadically (Figure5, Plate VIII).

Age Interpretation Based On Palynological Data

In western and central Anatolia, there are a lot of earlyNeogene basins, and most of them have been studiedpalynologically (Benda 1971a, b; Benda et al. 1974;Akgün 1986, 1993; Akgün & Akyol 1987, 1992, 1999;Gemici et al. 1991; Ediger et al. 1996; Karayi¤it et al.1999; Akgün et al. 2000a, b; Kayseri & Akgün 2002,2003, 2005; Akgün & Kayseri 2004; Akgün et al. 2004,2007; Kayseri et al. 2006). The sporomorphassemblages determined in these studies contain quite alarge number of well-known and long-rangingsporomorphs. Based on palynological associations in theprevious studies, the stratigraphic importance andabundance of sporomorphs throughout the Mioceneperiod can be interpreted as follows:

(1) The Early Miocene: Spore species such asLeiotriletes microadriennis, L. maxoides maximus, L.maxoides maxoides, Verrucatosporites scutulum, V.alenius, V. favus were more abundant in theEocene–Oligocene. These species were observed to berare in the early Miocene, occurring with Baculatisporites,Cingulatisporites and Stereisporites. Laevigatosporiteshaardti species is extremely numerous butstratigraphically unimportant. Some angiosperm pollensuch as Plicapollis pseudoexelsus, Dicolpopolliskalewensis, Compositoipollenites minimus,Subtriporopollenites anulatus anulatus, Momipitespunctatus and M. quietus are rare in the Early Miocene.

Pollen species characteristic of the Oligocene, such asMediocolpopollenites compactus, Slowakipollishippophaeoides, Bohlensipollis hohli and A. Cyclops, werenot observed in Miocene rocks.

(2) The Middle Miocene:: Taxodiaceae, Pinus(haploxylon-type), Myricaceae, Carya, Alnus, Ulmus,Fagaceae, Quercus, Castanea, Cyrillaceae and Oleaceae ofangiospermae reach their highest relative abundance inthe Middle Miocene. These pollen are also observedduring the Oligocene and Miocene. Tricolpopolleniteshenrici was abundant in the Early Miocene, but rare in theMiddle Miocene and was accompanied by angiospermpollen. Poaceae, Asteraceae and Cichorieae of theherbaceous angiosperm pollen accompanied otherangiosperm pollen less abundantly.

(3) The Late Miocene: Species of herbaceousangiosperm pollen are variously observed. Herbaceoustaxa such as Umbelliferae and Chenopodiaceae wereabundant and accompanied Poaceae, Asteraceae andCichorieae, which were present from the Middle Miocene.

These interpretations show that sporomorphassociation A of the Samsun-Havza area is of latestBurdigalian age, sporomorph association B is indicatativeof an early–middle Serravalian age in the Çorum-Evlik,Ayva, Zambal, ‹kizler, Kumbaba, Dodurga, ‹ncesu, Alıcık,Sivas-Karagöl and Akalın areas and sporomorphassociation C is considered to be of latestSerravalian–earliest Tortonian age in the Sivas-Vasıltepearea.

Correlation of the Sporomorph Associations FromAnatolia

Palynological studies on the Turkish Miocene wereconcentrated in western Anatolia. In this area,palynological data obtained from central Anatolia in thisstudy have been correlated with palynological data fromother parts of Anatolia in order to resolve thestratigraphic position of the Miocene basins (Table 1).

The palynological biostratigraphic chart of theNeogene strata in the Aegean region was first establishedby Benda et al. (1974) and Benda & Muelenkamp (1990).They used spores and pollen assemblage biozones(sporomorph associations) for the biostratigraphicclassification of Late Oligocene to Pliocene strata. Bendaet al. (1974) recognized five sporomorph associations:


368

Figure 5. Relative abundances of defined taxa for the samples of central and western Anatolia (Akgün 1986, 1993; Akgün & Akyol 1992, 1999; Akgün et al. 2000a, 2002; Karayi¤it et al.1999).

369


371

Tabl

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Corr

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372

the Kale, Eskihisar, Yeni-Eskihisar, Kızılhisar and Akça(Figure 6). Their Eskihisar sporomorph assemblage wascharacterized by predominant Q. henrici, Q. microhenrici,R. pseudocingulum, T. microcoryphaeus-punctatusgroup, T. myricoides, bituitus-rurensis group, T. hiatus,

T. betuloides, U. undulosus, Osmundaceae,Polypodiaceae, Pinus-haploxylon type, A. verus, Picea-type, Asper-type group, Gramineae, Chenopodiaceae,Pinus-silvestris type, Nyssa-type, Liquidambar-type andrare Umbelliferae, Tsuga-type, Intratriporopollenites

sporomorph association A

sporomorph association C

Figure 6. Correlation chart illustrating the relative ages of sporomorph associations from Çankırı-Çorum and Sivas basins andcomparison of previous palynologic studies with this study (Benda & Meulenkamp 1990).


373

instructus, Corrugatisporites solidus, Divisisporitesmaximus, Cicatricosisporites dorogensis andTriplanosporites sinuosus. This sporomorph assemblagewas suggested as of middle Burdigalian–early Serravalianage by Benda et al. (1974) and Benda & Muelenkamp(1990). The Eskihisar sporomorph association of Bendaet al. (1974) has thus been defined for a long time.Abundance of angiosperm pollen in this sporomorphassociation such as Momipites punctatus andQuercopollenites henrici and rare spore species can beaccepted for the Early Miocene part. In the MiddleMiocene part, these spore species disappear and thepercentage of some angiosperm pollen decreases. Otherangiosperm pollen accompany these spore and pollenspecies. Furthermore, previous studies show thatUmbelliferae, Monocolpopollenites areolatus andInaperturopollenites emmaensis are rarely present in theEskihisar sporomorph assemblage of Benda et al. (1974).Therefore, observing these spores and pollen together isproblematic in interpreting the stratigraphicaldistributions of these sporomorphs. Climatic changesoccurred throughout the Miocene period (Mosbrugger etal. 2005), and are reflected by the sporomorphassemblages. For this reason, if the time interval of Bendaet al. (1974)’s Eskihisar sporomorph assemblage isdivided into a lower and an upper part, these separationswill be enabled to correct age. Stratigraphical importance,presence and abundance of the spores and pollen speciesin our study show that the Samsun-Havza sporomorphassemblage resembles the Early Miocene part of theEskihisar sporomorph assemblage. The Kulo¤ulları-Baflçayır sporomorph assemblage (Büyük MenderesGraben), of early Middle Miocene age, is characterized byrare spore diversity. Moreover, some angiosperm speciesof the Oligocene–Miocene epochs were not observed in

the Kulo¤ulları-Baflçayır sporomorph assemblage. Hencethe Samsun-Havza sporomorph assemblage must beolder than the Kulo¤ulları-Baflçayır sporomorphassemblage (Table 1).

In this study, sporomorph association B of the Çorumregion and Karagöl, Akalın areas in the Sivas Basinindicates a Middle Miocene age. This sporomorphassemblage resembles the Soma, Akhisar-Çıtak, BüyükMenderes Graben, Ankara, Isparta, Kırflehir, Konya-Ilgınand Yozgat sporomorph assemblages of western andcentral Anatolia during the Middle Miocene (Akgün 1986;Akgün & Akyol 1987, 1992, 1999; Ya¤murlu et al.1988; Karayi¤it et al. 1999; Akgün et al. 2002) (Table1).

Sporomorph association C in this study indicates alatest Serrravalian and earliest Tortonian age. The fewpalynological correlation studies of western and centralAnatolia (Akgün et al. 1995, 2000a; Ediger et al. 1996)(Table 2) were compared with regard to the relativefrequency of herbaceous angiosperm pollen, importantfor a Late Miocene assemblage (Table 2). Herbaceouspollen percentages of sporomorph association C in ourstudy resemble the lower association of the Kızılhisarsporomorph assemblage of Benda et al. (1974) andBenda et al. (1982). Sporomorph assemblages of theBüyük Menderes Graben, Kırflehir-Tuzköy, of latestSerravalian–earliest Tortonian age resemble sporomorphassociation C in our study. Ediger et al. (1996)palynologically studied the Alaflehir-Turgutlu region andreported that the Alaflehir-Turgutlu sporomorphassemblage resembled the Yeni-Eskihisar sporomorphassemblage of Benda et al. (1974). The herbaceous pollenspecies in the Alaflehir-Turgutlu sporomorph assemblageare less abundant than in sporomorph association C

Table 2. Relative percentage correlation of the herbaceous angiosperm pollen.

Benda et al. (1974, 1982)K›z›lhisar

Ediger et al.(1996)

AssociationYeni-Eskihisar lower

association

Akgün & Akyol(1999) Sart Member

(Yeni-Eskihisar)

Akgün et al.(1995)

Akgün et al.(2000a)

This Study‘sporomorphassociation C’

AGE

lateSerravalian-

early Tortonianearly-lateTortonian

earliest LateMiocene earliest Tortonian

latestSerravalian-

earliestTortonian

middleTortonian

(MN9-MN10)

earliestTortonian

Location Greece WesternAnatolia

Büyük MenderesGraben Alaflehir-Turgutlu K›rflehir-

Tuzköy Sivas-Hafik Sivas-Vas›ltepe

Poaceae 7.6 15 12 1.3 7.5 1 19

Asteraceae 0.5 0.6 0.3 2.4 1 9.75 1.5Chenopodiaceae 0.3 2.9 3 _ 8 14.75 5.5

Umbelliferae 0.1 0 0 0.6 _ 1 1


374

(Table 2), so the latter is younger. Akgün et al. (2000a)studied coal samples of the Sivas-Hafik region. The Hafiksporomorph assemblage is characterized by predominantAsteraceae and Cichorieae while Chenopodiaceae speciesand Umbelliferae and Poaceae are less abundant in thisassemblage. This suggests that the Hafik sporomorphassemblage is younger than the sporomorph association Cin our study (Table 2).

Correlation of the Sporomorph Assemblage FromEurope

Palynological studies of the Neogene coal deposits ofEurope have been described in many papers (e.g., Hochuli1978; Thiele-Pfeiffer 1980; Van de Weerd 1983;Planderová et al. 1992; Nagy 1992; Ashraf &Mosbrugger 1995, 1996). Our sporomorph associationsare correlated with the sporomorph associations ofprevious studies in Europe.

Hochuli (1978) studied fossil pollen and spores of theCentral and Western Paratethys in the upper Eocene toEarly Miocene. He defined seven palynological zones,namely the Paleogene-Zone 18 (Late Eocene), 19 (EarlyOligocene), 20a, 20b (Middle Oligocene) and Neogene-Zones I (Late Oligocene–Early Miocene), II (late EarlyMiocene=Ottnangian) and the Neogene–Ottnangian zone.Species of Schizaeaceae are always scarce. Angiospermand gymnosperm pollen is abundant in theNeogene–Ottnangian zone (Hochuli 1978), which ischaracterized by the pollen species Caryapollenitessimplex, Polyporopollenites stellatus, P. undulasus,Momipites punctatus, Slowakipollis sp., and by thescarcity of some spore species such as Leiotriletesmaxoides, L. wolffi, Triplanosporites sinosus, T.microsinosus, Trilites multivallatus and Verrucatosporitesfavus. Sporomorph association A in this study includessporadic Lower Tertiary forms such as Leiotriletesmicroadriennis, Echinatisporites longiechinatus,Stereisporites stereoides ssp. stereoides, S. stereoidesssp. macroides and Polypodiaceoisporites cf. saxonicus.Therefore, sporomorph association C in the Samsun-Havza region is latest Burdigalian in age, and youngerthan the Neogene–Ottnangian zone sporomorphassemblage.

Thiele-Pfeiffer (1980) investigated the systematicdescription and stratigraphical interpretation of theMiocene microflora from the brown Coal opencast Odermine near Wackersdorf-Oberpflaz. The microflora of

Oder is compared with the others of the Neogene fromnorth, middle and east Europe. The results indicate thatthe Wackersdorf brown Coal was formed duringOttnangian–Badenian times. The Wackersdorfsporomorph assemblage of Ottnangian age includesLower Tertiary (Eocene–Oligocene) species. Sporomorphassociation A in our study includes sporadic lowerTertiary (the Late Oligocene–Early Miocene) species.Sporomorph association A is therefore younger thanThiele-Pfeiffer’s (1980) sporomorph association ofOttnangian age. The other sporomorph assemblage ofThiele-Pfeiffer (1980) is of Badenian age, andcharacterized by Sparganiaceae, Gramineae, Myricaceae,Pterocarya, Carya, Castaneae and Quercus. Sporomorphassociation B in our study resembles Thiele-Pfeiffer(1980) Badenian sporomorph assemblage, but lacksLeiotriletes wolfii, Cicatricosisporites chattensis andTrilites multivallatus.

Van de Weerd (1983) made a palynological study ofLate Miocene–Pliocene formations in Kastellious Hill(Greece), assigning this assemblage a Late Miocene toPliocene age. Sporomorph association C is recognized bysparse Monoporopollenites gramineoides (12%),Graminiidites laevigatus (1.5%), G. subtiliglobosus (1%),G. parvus (1%), Tricolporopollenites sp. (Asteraceae ‘1%’and Cichorieae ‘0.5%’ types), Umbelliferaepollenites sp.(0.5%), Periporopollenites multiporatus (4.5%) and P.halifani (1%). As these species are more abundant in theKastellious Hill sporomorph assemblage than in oursporomorph association C, the former sporomorphassemblage is younger.

Planderová et al. (1992) determined eight microfloralzones from the Egerian to the end of the Pliocene(MF1–MF9) in Slovakia. The Carpathian sporomorphassemblage indicates an assemblage zone MF5, which issimilar to the sporomorph association A in our study.Planderová’s (1991) Badenian sporomorph associationincludes Myricaceae, Ulmus, Engelhardtia, Betula, Picea,Abies, Carpinus, Ulmus, Quercus, Alnus and Pinus (MF6),and resembles sporomorph association B in our study.The Sarmatian sporomorph association (MF9) isdetermined by Pityosporites labdacus, Tusugaepollenitesigniculus, Betulaepollenites betuloides, Chenopodipollismultiplex, Artemisia, Poaceae, Asteraceae and Cichorieae,and is correlated with sporomorph association C thatincludes similar species (except Artemisia).

TAXA PREFERABLE HAB‹TAT CLIMATIC DISTRIBUTION PALAEOTROPIC/

ARCTOTERTIARY

SPORESSchizaeaceae/Lygodium ? Swamp Vegetation Subtropical to Tropical Palaeotropic

Gleicheniaceae ? Swamp Vegetation Subtropical-Tropical to WarmTemperate

Palaeotropic

Sphagnaceae Freshwater Plant Subtropical to Tropical PalaeotropicPolypodiaceae /Pteridoidreae Swamp or Riparian Vegetation Cosmopolitan

Osmundaceae/Osmunda Swamp or Riparian Vegetation CosmopolitanSelaginellaceae/Selaginella Riparian Vegetation Warm Temperate Arctotertiary

POLLENGYMNOSPERM

Pinus (haploxylon-type) Mixed Mesophytic Vegetation Warm Temperate ArctotertiaryPinus (silvestris-type) Mixed Mesophytic Vegetation Temperate Arctotertiary

Podocarpaceae / Podocarpus Mixed Mesophytic Vegetation Subtropical to Tropical PalaeotropicAbies Mixed Mesophytic Vegetation Temperate Arctotertiary

Taxodiaceae/Cupressaceae Mixed Mesophytic Vegetation Warm Temperate to Temperate ArctotertiaryTaxodiaceae Swamp Vegetation Warm Temperate Arctotertiary

Larix Swamp Vegetation Warm Temperate ArctotertiarySequoia Riparian Vegetation Warm Temperate ArctotertiaryEphedra Open Vegetation Temperate Arctotertiary

ANGIOSPERMMONOCOTYLEDONEAE POLLEN

Poaceae Open Vegetation CosmopolitanLemnaceae Freshwater Plant Cosmopolitan

Sparganiaceae/Sparganium Swamp Vegetation Temperate ArctotertiaryNymphaeaeae Freshwater Plant CosmopolitanCycadaceae Mixed Mesophytic Vegetation Subtropical to Tropical PalaeotropicArecaeae Mixed Mesophytic Vegetation Subtropical to Tropical Palaeotropic

DICOTYLEDONEAE POLLENMyricaceae/Myrica Swamp Vegetation Warm Temperate Arctotertiary

Juglandaceae/Engelhardtia Mixed Mesophytic Vegetation Subtropical to Tropical PalaeotropicBetulaceae/Corylus Mixed Mesophytic Vegetation Temperate Arctotertiary

Betulaceae Mixed Mesophytic Vegetation Temperate ArctotertiaryUlmaceae Mixed Mesophytic Vegetation Temperate Arctotertiary

Saxifragaceae/Itea Mixed Mesophytic Vegetation Cosmopolitan (North Temperate Zone)Rhamnaceae Mixed Mesophytic Vegetation Cosmopolitan

Juglandaceae/Platycarya Mixed Mesophytic Vegetation Temperate ArctotertiarySymplocaceae Mixed Mesophytic Vegetation Subtropical to Tropical PalaeotropicTiliaceae/Tilia Mixed Mesophytic Vegetation Temperate Arctotertiary

Carya Mixed Mesophytic Vegetation Temperate ArctotertiaryOnagraceae ? Swamp Vegetation Temperate Arctotertiary

Betulaceae/Alnus Swamp or Riparian Vegetation Temperate ArctotertiarySterculiaceae/ Reevesia Mixed Mesophytic Vegetation Subtropical to Tropical Palaeotropic

Myrtaceae Riparian Vegetation Subtropical to Tropical PalaeotropicJuglandaceae/Juglans Mixed Mesophytic Vegetation Temperate Arctotertiary

Ulmaceae, Ulmus; Zelkova Mixed Mesophytic Vegetation Temperate ArctotertiaryCarpinus Mixed Mesophytic Vegetation Temperate Arctotertiary

Pterocarya Riparian or Mixed Mesophytic Vegetation Warm Temperate ArctotertiaryFagaceae/Quercus Mixed Mesophytic Vegetation Warm Temperate to Temperate ArctotertiaryPlatanus and Salix Riparian Vegetation Temperate Arctotertiary

Castanea Mixed Mesophytic Vegetation Warm Temperate ArctotertiaryCyrillaceae Mixed Mesophytic Vegetation Subtropical to Tropical Arctotertiary

Anacardiaceae/Rhus Mixed Mesophytic Vegetation Warm Temperate ArctotertiarySimaroubaceae Riparian Vegetation Subtropical to Tropical Palaeotropic

Araliaceae Riparian or Mixed Mesophytic Vegetation CosmopolitanVitaceae Riparian Vegetation Subtropical to Tropical Palaeotropic

Nyssaceae/Nyssa Swamp Vegetation Subtropical to Tropical PalaeotropicSambucus Riparian Vegetation Temperate Arctotertiary

Aquifoliaceae/Ilex Mixed Mesophytic Vegetation Warm Temperate ArctotertiaryOleaceae/Olea Mixed Mesophytic Vegetation Subtropical to Tropical PalaeotropicUmbelliferae Open Vegetation Cosmopolitan

Asteraceae (Tubulifloreae and Ligulifloreaetypes)

Open Vegetation Cosmopolitan

Geraniaceae Open Vegetation Subtropical to Temperate PalaeotropicCaprifoliaceae/Lonicera Riparian or Mixed Mesophytic Vegetation Warm Temperate to Temperate Arctotertiary

Sapotaceae Mixed Mesophytic Vegetation Subtropical to Tropical PalaeotropicPolygalaceae Open Vegetation Cosmopolitan

Hamamelidaceae/Liquidambar Riparian Vegetation Warm Temperate ArctotertiaryChenopodiaceae Open Vegetation Cosmopolitan

ALGAEBotryococcus braunii Freshwater Cosmopolitan

Pediastrum sp. Freshwater Cosmopolitan


375

Table 3. Ecological requirement and climatic character of extant taxa represented by sporomorphs of the Çorum region and Sivas Basin (modifiedfrom Kovar-Eder 1987; Nagy 1990, 1999, 1992; Planderová 1991; Akgün & Akyol 1999).

Palaeoclimatology of the Çorum Region and SivasBasin

Climatic change in Europe during the Miocene is inferredto begin with a warm subtropical climate with manytropical elements in the Early Miocene. Subtropicalelements were dominant in the climate, but in the MiddleMiocene there was a gradual increase in temperateelements, and the tropical elements disappeared.Temperate elements become dominant in the LateMiocene, when the climate had become warm temperate(Benda et al. 1974; Kovar-Eder 1987; Benda &Muelenkamp 1990; Planderová 1991; Nagy 1992, 1999;Akgün & Akyol 1999). Additionally, the botanicalaffinities of the defining sporomorph associations in thestudy are grouped as palaeotropical (P) and arctotertiary(A) elements. Thus, we provide information aboutchanges in the ratio of palaeotropical to arctotertiaryelements (P/A-ratio), which presumably reflects climaticand vegetational changes in the Çorum region andGemerek area in the Sivas Basin. According to thesporomorph associations described in this study, theclimate change can be summarized as follows (Table 3).

Sporomorph association A is characterized byabundant subtropical to tropical elements such asSchizaeaceae, Lycopodia, Sapotaceae, Cycadaceae,Simaroubaceae, Cyrillaceae, Myrtaceae, Reevesia andPodocarpus, and includes fewer abundant warmtemperate and temperate and arctotertiary elements suchas Pinus (haploxylon-type), Taxodiaceae, Carya, Juglans,Betulaceae, Alnus, Tilia, Quercus, Platanus/Salix andCastanea, which accompany the subtropical and tropicalelements. Therefore sporomorph association A indicatesthat the climate was warm-subtropical during the latestBurdigalian in the Samsun area (Table 3, Figure 7).

Sporomorph association B of the Çorum region andGemerek area is represented by high percentages ofsubtropical elements such as Cycadaceae, Cyrillaceae,Simaroubaceae and Nyssa. Warm temperate andtemperate elements accompanying the subtropical andtropical elements include Pinus, Castanea, Rhus,Betulaceae, Ulmus, Quercus, Fagaceae, Liquidambar,Abies, Corylus, Carpinus, Tilia and Platycarya.Palaeotropical elements are scarcer in this sporomorphassociation. However, arctotertiary elements of thisassociation are more abundant than in sporomorphassociation A. Consequently, sporomorph association B

indicates that the climate was subtropical during theearly–middle Serravalian in the Çorum-Evlik, Ayva,Zambal, ‹kizler, Kumbaba, Dodurga, ‹ncesu Alıcık,Karagöl and Akalın areas (Table 3, Figure 7).

Sporomorph association C is recognized by abundantwarm temperate and temperate elements (arctotertiary)such as Pinus, Sequoia, Myricaceae, Castanea, Betulaceae,Ulmus, Quercus, Platanus/Salix, Ilex, Fagaceae,Liquidambar, Abies, Corylus, Carpinus, Sambucus andTilia. Subtropical to tropical elements preservedsporadically in sporomorph association C includeCycadaceae, Cyrillaceae, Reevesia and Sapotaceae.Palaeotropical elements of this sporomorph associationare scarcer. At the same time herbaceous(Chenopodiaceae, Poaceae, Asteraceae, Cichorieae,Ephedraceae and Umbelliferae) taxa are abundant. Forthese reasons, sporomorph associaton C in the Sivas-Vasıltepe region suggests that a warm temperate climateprevailed between the latest Serravalian and earliestTortonian (Table 3, Figure 7).

Palaeovegetation of the Çorum Region and SivasBasin

Botanical affinities of defining sporomorphs in the Çorumregion and Gemerek area in the Sivas Basin have beendefined, and these are grouped into palaeovegetationaltypes. Palaeovegetational differences between westernand central Anatolia have also been determined. Definingspores and pollen in our study are grouped undervegetational types such as montane (including mountainforest elements), mixed mesophytic forest (consisting ofdecidous and evergreen trees), lowland-riparian, swamp-freshwater and open vegetation (Table 3).Palaeovegetation of the Çorum and Gemerek regions willbe reconstructed for the Middle–early Late Mioceneperiods using these vegetational types.

Information about the composition and characteristicfeatures of the vegetation during the latest Burdigalian isobtained from pollen diagrams of the Samsun-Havzaregion. Characteristic of the vegetation of that time is theregular occurrence and abundance of thermophilousspecies like Engelhardtia, Sapotaceae, Reevesia,Schiazaceae and Gleicheniaceae. Together with therelatively high P/A–ratio, this suggests a warmsubtropical climate during the latest Burdigalian.


376


377

Correspondingly, the arctotertiary elements of the mixedmesophytic forest such as Juglandaceae, Tilia, Carya,Ulmus and Carpinus are less abundant. The swamp forestwas also well developed during the latest Burdigalian. Itscomponents, such as Taxodiaceae, Nyssa and Myricaceaeshow comparatively high values in the pollen spectra.Probably the relief and palaeogeographic situation of thattime indicated the wide distribution of the swamp forestand of the ecologically related riparian forest withPlatanus/Salix, Ulmus, Carya and Pterocarya (Table 3,Figure 8).

Sporomorph association B is defined from the Çorum-Evlik, Ayva, Zambal, ‹kizler, Kumbaba, Dodurga, ‹ncesuand Alıcık and Sivas-Karagöl, Akalın in the Çorum andGemerek areas. During the early–middle Serravalianperiod in the Çorum and Gemerek regions in the SivasBasin the swamp, montane and mixed mesophytic forestelements were abundant, indicating a subtropicalcharacter. However, the swamp forest element occursmore abundantly in samples from the Kumbaba and‹skilip-Çomu regions, regardless of the mountain forestelements, which are less abundantly seen in samples from

(This study)

a)

Figure 7. The relative percentage of the palaeotropical and arctotertiary elements derived from the samples of central Anatolia and correlatedwith previous studies (Nagy 1990; Planderova 1991 and Syabryaj 2002). (A) Long-term trends in benthic oxygen isotope rations(Zachos et al. 2001).


378

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379

these regions. The high percentage of mixed mesophyticforest element is accompanied by swamp and montaneforest associations. Each forest element is more abundantin the sporomorph associations from the Evlik, ‹kizler,Dodurga, Kumbaba, Alıcık, Karagöl and Akalın areas.Results from sporomorph association B, suggest thatpalaeovegetation from the ‹skilip-Çomu and Kumbabaareas indicates widespread lacustrine environments.Other regions are characterized by lacustrineenvironments surrounded by mountains (Table 3, Figure8).

During the earliest Tortonian the vegetation of theSivas-Vasıltepe region was not different from that inlatest Burdigalian and early–middle Serravalian times.Percentages of swamp, riparian and mixed mesophyticforests resemble each other in sporomorph association Cin the Sivas-Vasıltepe region. The herb species of openvegetational environments accompany the forestassociations. The variable dominance of elementsbelonging to open vegetation, especially Poaceae,Chenopodiaceae, Umbelliferae, Asteraceae, Cichorieaeand Ephedraceae clearly demonstrate that grasslandhabitats were extensive during the early and middleTortonian. This indicates that these habitats probablyexisted side by side in open vegetation. High ground wasalso covered by Pinus, Picea, Abies, Podacarpus, Corylus,Betulaceae, Carya, Engelhardtia, Juglans, Cupressaceae,Carpinus, Araliaceae, Ulmus/Zelkova, Pterocarya,Quercus, Arecaceae, Castanea, Platycarya,Anacardiaceae/Rhus, Reevesia, Carpinus, Oleaceae, Ilex,Fagaceae, Sambucus and Tilia (Table 3, Figure 8).

Palynological studies so far show that thepalaeoenvironment during the Miocene in westernAnatolia was characterized by broad, permanent lakes.Palaeovegetation indicating low palaeotopographiccondition surrounded these lakes. The definingpalaeovegetation of the Çorum and Gemerek regions isdifferent from that of western Anatolia. Early–middleSerravalian vegetation in central Anatolia indicates alacustrine environment in high topographic conditions,with lakes among the mountains (Figures 8 & 9).Palynological and mammalian data show that thesepalaeovegetational conditions continued into the earlyTortonian (Geraads et al. 2005).

The sporomorph contents of the early–middleSerravalian in the Çorum region, the Sivas Basin and the

Yozgat-Yerköy region have been evaluated by detrendedcorrespondence analyses. Thus, reconstruction of thepalaeovegetation during the early–middle Serravalian incentral Anatolia can be obtained. In the Yozgat-Yerköyregion, the Sivas Basin and the Çorum region samplesplot on the positive part of Axis 1 and 2. Samples fromthe Gemerek region in the Sivas Basin and Çorum regionshave been gathered from areas with swamp and freshwater palaeocommunities. The Yozgat-Yerköy samplesand a few Çorum region samples have been groupedunder the field characterized by montane and riparian-lowland palaeocommunities. Most of the Çorum regionsamples have been assembled in an area of riparianlowland, mixed mesophytic and swamppalaeocommunities. These results show that the Yozgat-Yerköy region had high palaeotopography during theearly–middle Serravalian, although the Çorum area had ahigher palaeotopography than the Yozgat region, becausethe samples collected from the Çorum region were closeto the mixed mesophiytic palaeocommunity. Samplesfrom the Çorum region indicate a lacustrine environmentsurrounded by the mountains (Figure 10). Samples fromthe Sivas Basin show that it was characterized by swampforest at this time.

Palaeoclimatic Reconstructions with theCoexistence Approach Method (CA)

The CA is a computer-aided technique for quantitativeterrestrial climate reconstructions in the Tertiary usingplant fossils. In this study, differences of the MART valuesrelating to the palaeotopography (Sezer 1990) areexamined. Palaeotopography reflections on thepalaeoclimate are deduced using the MART values in thispart.

The sporomorph data from the latest Burdigalianwere obtained from the Samsun-Havza region in centralAnatolia. The palaeoclimatic parameters are based on the29 taxa in samples from that region. The resultingcalculations are 19 °C for MAT, 9.75 °C for the CMT,27.7 °C for the WMT, 1217 to 1322 mm for the MAPand 17.45 °C for the MART, respectively (Table 4).

The MAT values for the early–middle Serravalian inthe Çorum region and the Sivas Basin generally rangebetween 18–19 °C. However, while the MAT value forthe Dodurga region is clearly low (10.05 °C), the MART


380

values are high (Table 4, Figure 8). Generally, the CMTvalues for the early–middle Serravalian are variable in CA,based on results from samples in the Çorum and Gemerekregions (10.55–(-0.8) °C). The CMT results show that, ifthe swamp forest elements have a high percentage in thesamples, values of the CMT are increased and the MARTvalues are decreased. This evidently shows that a swamp

environment is caused by warm climatic conditions. Whilethe WMT values of samples in the Çorum and Gemerekregions range between the 26–27 °C, the results fromthe Dodurga region are 10.05 °C for the MAT, -0.8 °Cfor the CMT, 24.7 °C for the WMT and 25.5 °C for theMART. These different results of Dodurga region samplesrelate to its high elevation at the time.

w

s

Figure 9. Palaeoenvironment reconstruction of Çorum region and Sivas Basin during the deposition of the Middle and earliest Late Miocene.


381

The earliest Tortonian assemblage was determined inthe Sivas-Vasıltepe (Gemerek) region. 37 taxa wererecorded. Palaeoclimatic parameters are based on 20 taxafor the earliest Tortonian. The results are 19 °C for theMAT, 9.4 °C for the CMT, 27.7 °C for WMT and 1187to 1574 mm for the MAP, respectively (Table 3). HighMART values from the Gemerek region in the Sivas Basinindicate high elevation. From the early–middle Serravalianto the early Tortonian, the climate changed fromsubtropical to warm temperate, causing a decrease of theCMT of about 2 °C in the Gemerek region (Table 4).

The high MART values in the Middle and early LateMiocene samples reflect the high elevation, because themountain and mixed mesophytic forest elements of thesesamples are abundant compared to the percentage of theswamp forest elements. This environmental difference is

caused by the diversity of the regional climate (Table 4,Figure 8).

The combined approach results from the Çorum andGemerek regions have been correlated with the resultsfrom Germany, Bulgaria and Armenia (Bruch &Gabrielyan 2001; Syabryaj 2002; Mosbrugger et al.2005). From the late Burdigalian to the middleSerravalian the MAT values are high, but in the lateSerravalian a decrease occurs. The MAT values ofGermany, Bulgaria and Armenia are generally lower thanthose of central Anatolia during the Middle Miocene(Bruch & Gabrielyan 2001) (Figures 7 & 11) and thehigher MAT values of central Anatolia can be related tothe relative palaeogeographical position of these countriesin the Middle Miocene. Mosbrugger et al. (2005) andAlexsandrove et al. (1987) stated that the succeeding

r

r

Figure 10. Samples and palaeocommunities for Çorum region and Sivas Basin during the early and middle Serravallian represented by in thespace of the two first axes using detrended correspondence analysis.


382

warm time span persisted through the earlier part of theSerravalian, and corresponds to the Middle MioceneClimatic Optimum that is also observed globally. TheMiddle Miocene Climatic Optimum is reflected byincreases of all the temperature records across centralEurope. For MAT and WMT, similar values were obtainedfrom our palynoflora of different samples during thattime. The CMT results are 9–13 °C for Lausitz and LowerRhine basins in central Europe. According to theMosbrugger et al. (2005), high CMTs mark the MiddleMiocene Climatic Optimum in Europe. The MiddleMiocene (late Early to early Middle Miocene) thermaloptimum has been discussed by many workers inAmerica, all of whom have certainly known that MATvalues peaked during this interval and then began adecline (Wolfe 1979, 1994) (Figure 7A). During the lateEarly to early Middle Miocene, the CMT results forEurope are calculated at between 8 and 10 °C. However,CMT results from central Anatolia in the early–middle

Serravalian are low ((-0.8)–7.8 °C) and these lower CMTresults can mark the cooling palaeoclimate in Europe andAmerica (from the late Langhian to earliest Serravalian).

While CA results (MART, MAT, CMT, WMT and MAP)are correlated with the recent climatic data of the Çorumarea and the Gemerek region in the Sivas Basin, it can besaid that all climatic variables distinctly decrease. MARTvalues indicate that high elevation of the Dodurga regionwas initiated during the Middle Miocene and this hascontinued till recent times. Additionally decreasing MAPvalues clearly indicate the present dry climate (Table 4).

Conclusions

The results of this study are as follows: (1) this is the firstdetailed palynological study in the Miocene sediments ofcentral Anatolia. The palynostratigraphical results arecorrelated with previous studies of western and centralAnatolia; (2) three sporomorph associations have been

MAP (mm)AGE LOCATION MART(oC)

MAT(oC)

CMT(oC)

WMT(oC)

MAP(min)

MAP(max)

early Burdigalian SAMSUN-HAVZA 17,45 19 9,75 27,2 1217 1322

ÇORUM-ALICIK 17,2 19,1 10,5 27,7 1187 1355

ÇORUM-AYVA 19,8 19 7,8 27,6 1187 1520ÇORUM-DODURGA 25,5 10,05 -0,8 24,7 1122 1520

ÇORUM-EVL‹K 22,1 19 5,6 27,7 1217 1322ÇORUM-‹K‹ZLER 20 18,9 7,8 27,8 887 1613ÇORUM-‹NCESU 20,3 19,15 7,1 27,4 1146 1322ÇORUM-‹SK‹L‹P 18,3 18,9 9,4 27,7 1122 1520

ÇORUM-KUMBABA 19,8 18,65 7,8 27,6 887 1520ÇORUM-ZAMBAL 19,9 18,8 7,8 27,7 1122 1355

S‹VAS-KARAGÖL/AKALIN 17,15 19,1 10,55 27,7 823 1574

early-middle Seravalian

YOZGAT-YERKÖY 15,6 16,85 11,15 26,75 735 1520early Tortonian S‹VAS-VASILTEPE 18,3 19 9,4 27,7 1187 1574

LOCATIONMART

(oC)MAT(oC)

CMT(oC)

WMT(oC)

MAP(mm)

SAMSUN-HAVZA 16,07 14,34 6,97 23,04 707,8

ÇORUM-DODURGA 20,58 10,62 -0,42 21,00 424,2

ÇORUM-‹SK‹L‹P 20,58 10,62 -0,42 21,00 424,2

S‹VAS-KARAGÖL/AKALIN 16,52 8,18 -3,44 19,96 426,8

Recent

YOZGAT-YERKÖY 17,42 8,24 -2,03 19,45 582,1

Table 4. Values for the Coexistance Approach Analysis of the Çank›r› region and Sivas Basin and recent climatic temperature values ofÇorum and Sivas regions.


383

(This study) Germany (Mosbrugger 2005)et al.Bulgaria (Ivanov 2002)et al.Armenia

Bruch & Gabrielyan 2001

Figure 11. Correspondence analysis data (MAT, CMT, WMT and MAP) of central Anatolia compared with the dataof neighboring countries (Germany, Armenia and Bulgaria).

defined in this study. Sporomorph association A ofSamsun-Havza region is latest Burdigalian in age.Sporomorph association C of the Çorum-Evlik, ‹kizler,Kumbaba, Dodurga, Ayva, Amasya-Çomu areas (in theÇorum region) and the Sivas-Gemerek-Karagöl, Akalınareas is of early–middle Serravalian age. Sporomorphassociation C of Sivas-Vasıltepe (Gemerek) area is ofearliest Tortonian age; (3) the sporomorph association of

the Samsun-Havza area is characterized by a warmsubtropical climate and CA results are:- for the MAT 19°C, for the CMT 9.75 °C, for the WMT 27.2 °C, for theMAP 1217–1322 mm and the MART 17.45 °Crespectively; (4) the sporomorph association from theÇorum and Gemerek regions in the Sivas Basin indicatesa subtropical climate. The CA results of this sporomorphassociation are for the: (i) MAT 18–19.15 °C, (ii) CMT (-


384

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Acknowledgements

The authors are grateful to Zeki Atalay (GeneralDirectorate of Mineral Research and Exploration ‘MTA’)and ‹brahim Türkmen (Fırat University) who supplied thesamples of this study. They would like to thank EcmelErlat (Ege University) for suggestions regarding therecent climatic condition of Turkey. The authors wouldalso like to thank Alfred Traverse, Mike Pole, Volkan fi.Ediger, Erdin Bozkurt and Turushan Kayseri forimproving the text and correcting the English. Financialsupport was provided by Dokuz Eylül University,Graduate School of Natural and Applied Science projectnumbers: 02KB.FEN.046, which was are M.Sc. project ofMine Sezgül Kayseri. The authors are indebted to theNECLIME programme (Neogene climate evolution inEurasia) for the invitation to participate in severalinternational workshops. John A. Winchester editedEnglish of the final text.


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RÜCKERT-ÜLKÜMEN, N.V. 1998. Cyprinidae (Pisces) aus dem JungtertiärVon Alpagut-Dodurgabei Çorum (Mittelanatolien, Turkei).Mitteilungen Bayer Staatsslg. Paläontologie Historical Geology38, 167–181.

fiEN, fi., SEY‹TO⁄LU, G., KARADEN‹ZL‹, L., KAZANCI, N., VAROL, B. & ARAZ, H.1998. Mammalian biochronology of Neogene deposits and itscorrelation with the lithostratigraphy in the Çankırı-Çorum basin,central Anatolia, Turkey. Eclogae Geologicae Helvetiae 91,307–320.

fiENGÖR, A.M.C. & YILMAZ, Y. 1981. Tethyan evolution of Turkey: a platetectonic approach. Tectonophysics 75, 181–241.

SEYMEN, ‹. 1981. Kırflehir dolayındaki Kırflehir Masifi’nin stratigrafisi vemetamorfizması [Stratigraphy and metamorphism of KırflehirMassif in Kırflehir area]. Bulletin of the Geological Society ofTurkey 24, 7–14 [in Turkish with English abstract].

SEZER, L.I. 1990. Türkiye’de ortalama yıllık sıcaklık farkının da¤ılıflı vekontinentalite derecesi üzerine yeni bir formül [Distribution of themean annual temperature in Turkey and a formula on thecontinentalite degree]. Aegean Geographical Journal 5, 110–159[in Turkish, unpublished].

PICER, R.A. & HILL, C.R. 1979. Principal components andcorrespondence analyses of quantitative data from a Jurassicplant bed. Review of Paleobotany and Palynology 28, 273–299.

SÜMENGEN, M., ÜNAY, E., SARAÇ, G., BRUIJN, H., TERLEMEZ, ‹. & GÜRBÜZ, M.1990. New Neogene Rodent assemblages from Anatolia (Turkey).In: LINDSEY, E.H., FALBUSCH, V., MEIN, P. (eds), European NeogeneMammal Chronology, Plenum Press, New York, 1989. GeneralDirectorate of Mineral Research and Exploration of Turkey,61–72.

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387

Received 5 December 2006; revised typescript received 25 June 2007; accepted 12 November 2007


388

PLATE I

(SAMSUN-HAVZA)(All illustrations X 500)

Figure 1. Leiotriletes microadriennis W. KRUTZSCH2. Brandenburgisporis beckwitzensis W. KRUTZSCH3. Stereisporites stereoides (R. POTONIÉ & VENITZ) THOMSON & PFLUG4. Stereisporites macroides W. KRUTZSCH5. Echinatisporites longiechinatus W. KRUTZSCH6,7. Baculatisporites primarius (WOLLF) THOMSON & PFLUG primarius W. KRUTZSCH8. Baculatisporites cf. nonus (WOLLF) W. KRUTZSCH ssp. cf. baculatus W. KRUTZSCH9. Laevigatosporites haardti (R. POTONIÉ & VENITZ) THOMSON & PFLUG 10,11. Pityosporites microalatus (R. POTONIÉ) THOMSON & PFLUG 12. Pityosporites labdacus THOMSON & PFLUG13. Inaperturopollenites dubius (R. POTONIÉ & VENITZ) PFLUG & THOMSON in THOMSON & PFLUG14,15. Inaperturopollenites hiatus (R. POTONIÉ) PFLUG & THOMSON in THOMSON & PFLUG16. Inaperturopollenites verrupapillatus TREVISAN17. Graminidites laevigatus W. KRUTZSCH18. Echigraminidites moravicus W. KRUTZSCH19. Sparganiapollenites neogenicus W. KRUTZSCH20–22. Triatriopollenites rurensis PFLUG & THOMSON in THOMSON & PFLUG23,24. Triatriopollenites bituitus (R. POTONIÉ) THOMSON & PFLUG25. Triatriopollenites corypheause (R. POTONIÉ) THOMSON & PFLUG26–29. Momipites punctatus (R. POTONIÉ) NAGY30. Triporopollenites coryloides PFLUG in THOMSON & PFLUG31. Triporopollenites simpliformis PFLUG & THOMSON in THOMSON & PFLUG32. Triporopollenites fragilis NAKOMAN33. Triporopollenites sp.34. Intratriporopollenites indubitalibis (R. POTONIÉ) PFLUG & THOMSON in THOMSON & PFLUG35. Subtriporopollenites simplex (R. POTONIÉ & VENITZ) THOMSON & PFLUG 36. Subtriporopollenites anulatus (R. POTONIÉ & VENITZ) THOMSON & PFLUG37. Corsinipollenites occulis ssp. noctis (THIERGART) NAKOMAN38. Polyporopollenites undulosus (WOLFF) THOMSON & PFLUG 39. Polyporopollenites carpinoides PFLUG & THOMSON in THOMSON & PFLUG40. Polyporopollenites stellatus (R. POTONIÉ & VENITZ) THOMSON & PFLUG41. Myrtaceidites mesonesus COOKSON & PIKE42,43. Reevesiapollis triangulus (MAMCZAR) W. KRUTZSCH44. Tricolpopollenites henrici (R. POTONIÉ) THOMSON & PFLUG45–48. Tricolpopollenites microhenrici (R. POTONIÉ) THOMSON & PFLUG49,50. Tricolpopollenites densus PFLUG in THOMSON & PFLUG51. Tricolpopollenites retiformis PFLUG & THOMSON in THOMSON & PFLUG52–54. Tricolporopollenites cingulum (R. POTONIÉ) THOMSON & PFLUG55,56. Tricolporopollenites megaexactus (R. POTONIÉ) THOMSON & PFLUG57,66. Tricolporopollenites steinensis (R. POTONIÉ) THOMSON & PFLUG58–61. Tricolporopollenites krucshi (R. POTONIÉ) THOMSON & PFLUG ssp. rodderensis THIERGART62–65. Tricolporopollenites microreticulatus PFLUG & THOMSON in THOMSON & PFLUG67,68. Tricolporopollenites microellipsus PFLUG in THOMSON & PFLUG69. Tetracolporopollenites abditus PFLUG in THOMSON & PFLUG70. Periporopollenites halifani NAKOMAN71. Juglandaceapollenites verus RAATZ72. Pediastrum73. Botryococcus brunii KÜTZING


389

1 2

3

45 6

36

7

89

1011 12

13 14 15 1618 19 20

21 22 23 2425 26

17

27 28 29

30 3132 33 34

3537

3839

40

4142 43 44

45 46

47 48 49 50 5152 53 54 55 56 57

58 59

6061 62 63 64 65

66 67 68 6970

71 7273


390

PLATE II

(ALICIK)(All illustrations X 500)

Figure 1,2. Laevigatosporites haardti (R. POTONIÉ & VENITZ) THOMSON & PFLUG 3,4. Pityosporites strobipites (WODEHOUSE) W. KRUTZSCH5. Cupressacidites cuspidateaformis (ZAKLINSKAJA) W. KRUTZSCH6. Inaperturopollenites verrupapillatus TREVISAN7. Graminidites laevigatus W. KRUTZSCH8,9. Graminidites subtiliglobosus W. KRUTZSCH10,11. Graminidites pseudogramineus W. KRUTZSCH12,13. Echigraminidites moravicus W. KRUTZSCH14,15. Sparganiapollenites neogenicus W. KRUTZSCH16. Cycadopites sp.17–20 Triatriopollenites rurensis PFLUG & THOMSON in THOMSON & PFLUG21,22 Triatriopollenites bituitus (R. POTONIÉ) THOMSON & PFLUG23 Subtriporopollenites simplex (R. POTONIÉ & VENITZ) THOMSON & PFLUG24,25 Intratriporopollenites instructus (R. POTONIÉ) THOMSON & PFLUG26,27 Polyporopollenites stellatus (R. POTONIÉ & VENITZ) THOMSON & PFLUG28–31. Porocolpopollenites sp.32,33. Tricolpopollenites henrici (R. POTONIÉ) THOMSON & PFLUG34–37. Tricolpopollenites microhenrici (R. POTONIÉ) THOMSON & PFLUG38. Quercopollenites robur PLANDEROVÁ39,40. Tricolpopollenites microhenrici R. POTONIÉ ssp. medius ZONGHAO41–45. Tricolporopollenites cingulum (R. POTONIÉ) THOMSON & PFLUG 46–49. Tricolporopollenites megaexactus (R. POTONIÉ) THOMSON & PFLUG 50. Tricolporopollenites pacatus PFLUG in THOMSON & PFLUG51. Tricolporopollenites microreticulatus PFLUG & THOMSON in THOMSON & PFLUG52. Tricolporopollenites margaritatus (R. POTONIÉ) THOMSON & PFLUG 53. Tricolporopollenites iliacus (R. POTONIÉ) ncomb. THOMSON & PFLUG 54. Rhuspollenites ornatus (THIELE–PFEIFFER) 55–59. Umbelliferaepollenites spp.60,61. Tricolporopollenites spp. (Asteraceae–Tubuliflorea type)62,63. Periporopollenites perpilexus NAKOMAN64. Tetracolporopollenites abditus PFLUG in THOMSON & PFLUG65–67. Periporopollenites halifani NAKOMAN68. Periporopollenites multiporatus PFLUG in THOMSON & PFLUG69. Periporopollenites stigmosus (R. POTONIÉ) THOMSON & PFLUG


391

1 2 3 4

56

7

8

910 11

12

13

14

15

16

18

19 20 21 2223

2425 26

17

2728 29 30 31

32 3334 35

36 37 3839 40 41 42 43 44 45 46

47 48 49 50 51 52 53 54 5556 57

58

59

60

61

62

63

64

65

66

67

6869


392

PLATE III

(‹SK‹L‹P)(All illustrations X 500)

Figure 1. Leiotriletes microadriennis W. KRUTZSCH2–4. Baculatisporites cf. nonus (WOLLF) THOMSON & PFLUG ssp. baculatus W. KRUTZSCH5. Punctatisporites micropunctatus W. KRUTZSCH6. Laevigatosporites gracilis WILSON & WEBSTER7. Pityosporites microalatus (R. POTONIÉ) THOMSON & PFLUG 8. Pityosporites labdacus THOMSON & PFLUG9. Abiespollenites absolutus (THIERGART) n.comb. W. KRUTZSCH10. Abiespollenites latisaccatus (TREVISAN) n.comb. W. KRUTZSCH11. Inaperturopollenites dubius (R. POTONIÉ & VENITZ) PFLUG & THOMSON in THOMSON & PFLUG12,13. Inaperturopollenites hiatus (R. POTONIÉ) PFLUG & THOMSON in THOMSON & PFLUG14. Graminidites subtiliglobosus W. KRUTZSCH15. Sparganiapollenites sparganoides (MEYER) W. KRUTZSCH16. Cycadopites sp.17. Monogemmites pseudosetarius WEYLAND & PFLUG18. Triatriopollenites rurensis PFLUG & THOMSON in THOMSON & PFLUG19. Triatriopollenites corypheause (R. POTONIÉ) THOMSON & PFLUG20. Triatriopollenites bituitus (R. POTONIÉ) THOMSON & PFLUG21–25. Momipites punctatus (R. POTONIÉ) NAGY26–28. Polyvestibulopollenites verus PFLUG in THOMSON & PFLUG29. Subtriporopollenites simplex (R. POTONIÉ & VENITZ) THOMSON & PFLUG 30,31. Polyporopollenites undulosus (WOLFF) THOMSON & PFLUG32,33. Polyporopollenites stellatus (R. POTONIÉ & VENITZ) THOMSON & PFLUG34,35. Tricolpopollenites microhenrici (R. POTONIÉ) THOMSON & PFLUG36–41. Tricolporopollenites megaexactus (R. POTONIÉ) THOMSON & PFLUG 42. Tricolporopollenites pacatus PFLUG in THOMSON & PFLUG43,44. Tricolporopollenites microreticulatus PFLUG & THOMSON in THOMSON & PFLUG45. Tricolporopollenites sp. (Avicennia type)46. Tricolporopollenites sp.47. Tetracolporopollenites abditus PFLUG in THOMSON & PFLUG48,49. Periporopollenites multiporatus PFLUG in THOMSON & PFLUG


393

1 23 4 5

6

36

7 8

9

10

11

12 13

14

1516

18

19 20 21 22 23 24 25 26

17

27

2829

3031

32 33

34 3537 38

39 40 41

42 43 44

45 46

47 48 49


394

PLATE IV

(‹K‹ZLER-DODURGA)(All illustrations X 500)

Figure 1. Trilites sp.2. Stereisporites (Stereoides) stereoides (R. POTONIÉ & VENITZ) THOMSON & PFLUG 3. Baculatisporites primarium (WOLLF) THOMSON & PFLUG ssp. primarius W. KRUTZSCH4,5. Laevigatosporites haardti (R. POTONIÉ & VENITZ) THOMSON & PFLUG 6,7. Pityosporites microalatus (R. POTONIÉ) THOMSON & PFLUG12. Pityosporites labdacus (R. POTONIÉ) THOMSON & PFLUG 9,10. Cycadopites spp.11. Arecipites sp.12–14. Inaperturopollenites hiatus (R. POTONIÉ) PFLUG & THOMSON in THOMSON & PFLUG15. Cupressacidites cuspidateaformis (ZAKLINSKAJA) W. KRUTZSCH16. Inaperturopollenites microforatus W. KRUTZSCH17,18. Inaperturopollenites polyformosus (THIERGART) THOMSON & PFLUG19–21. Graminidites laevigatus W. KRUTZSCH22,23. Sparganiapollenites polygonalis THIERGART24. Sparganiapollenites magnoides W. KRUTZSCH25. Sparganiapollenites neogenicus W. KRUTZSCH26,29. Triatriopollenites bituitus (R. POTONIÉ) THOMSON & PFLUG27,28. Triatriopollenites rurensis PFLUG & THOMSON in THOMSON & PFLUG30. Triporopollenites simpliformis PFLUG & THOMSON in THOMSON & PFLUG31–33. Polyvestibulopollenites verus PFLUG in THOMSON & PFLUG34,35. Subtriporopollenites simplex (R. POTONIÉ & VENITZ) THOMSON & PFLUG 36. Corsinipollenites occulis ssp. noctis (THIERGART) NAKOMAN37,38. Polyporopollenites undulosus (WOLFF) THOMSON & PFLUG 39,40. Polyporopollenites stellatus (R. POTONIÉ & VENITZ) THOMSON & PFLUG41,42. Tricolpopollenites henrici (R. POTONIÉ) THOMSON & PFLUG43. Tricolpopollenites microhenrici (R. POTONIÉ) THOMSON & PFLUG44. Tricolpopollenites densus PFLUG in THOMSON & PFLUG45–50. Tricolporopollenites cingulum (R. POTONIÉ) THOMSON & PFLUG 51–55,57. Tricolporopollenites megaexactus (R. POTONIÉ) THOMSON & PFLUG 56. Tricolporopollenites pacatus PFLUG in THOMSON & PFLUG58,59. Tricolporopollenites microreticulatus PFLUG & THOMSON in THOMSON & PFLUG60. Tricolporopollenites krucshi (R. POTONIÉ) THOMSON & PFLUG ssp. rodderensis THIERGART61. Tricolporopollenites krucshi (R. POTONIÉ) THOMSON & PFLUG ssp. pseudolaesus (R. POTONIÉ) THOMSON & PFLUG62. Tricolporopollenites oleoides W. KRUTZSCH & VANHOORNE63,64. Tricolporopollenites sp. (Asteraceae–Tubulifloreae type)65,66. Periporopollenites halifani NAKOMAN


395

1 2 3 4 5 6

36

78 9 10

11 12

13 14 1516 18 19 20

2122 23

24 25 26

17

27 28 29

30 31 32 33 34 35 37

38 3940 41

42 43 4445 46

47 48 49 50 51 52 53 54 55 56 57

58 59

60 6162

63 64 65 66


396

PLATE V

(AYVA-KUMBABA)(All illustrations X 500)

Figure 1,2. Stereisporites (Stereoides) stereoides (R. POTONIÉ & VENITZ) THOMSON & PFLUG ssp. stereoides W. KRUTZSCH3. Laevigatosporites pseudodiscordatus W. KRUTZSCH4,5. Pityosporites microalatus (R. POTONIÉ) THOMSON & PFLUG 6,7. Inaperturopollenites hiatus (R. POTONIÉ) PFLUG & THOMSON in THOMSON & PFLUG8. Inaperturopollenites polyformosus (THIERGART) THOMSON & PFLUG9. Cupressacidites cuspidateaformis (ZAKLINSKAJA) W. KRUTZSCH10,11. Graminidites laevigatus W. KRUTZSCH12,13. Monogemmites pseudosetarius WEYLAND & PFLUG14. Echigraminidites moravicus W. KRUTZSCH15. Sparganiapollenites sparganoides (MEYER) W. KRUTZSCH16. Triatriopollenites rurensis PFLUG & THOMSON in THOMSON & PFLUG17. Triatriopollenites bituitus (R. POTONIÉ) THOMSON & PFLUG18,19. Triatriopollenites coryphaeuse (R. POTONIÉ) THOMSON & PFLUG20–22. Momipites punctatus (R. POTONIÉ) NAGY23. Triporopollenites simpliformis PFLUG & THOMSON in THOMSON & PFLUG 24. Lonicerapollis cf. gallwitzi W. KRUTZSCH25. Reevesiapollis triangulus (MAMCZAR) W. KRUTZSCH26,27. Polyvestibulopollenites verus PFLUG in THOMSON & PFLUG28,29,31. Subtriporopollenites simplex (R. POTONIÉ & VENITZ) THOMSON & PFLUG 30. Polyporopollenites undulosus (WOLFF) THOMSON & PFLUG 32,33. Polyporopollenites carpinoides PFLUG & THOMSON in THOMSON & PFLUG34,35. Polyporopollenites stellatus (R. POTONIÉ & VENITZ) THOMSON & PFLUG36–41. Tricolpopollenites henrici (R. POTONIÉ) THOMSON & PFLUG42–45. Tricolpopollenites microhenrici (R. POTONIÉ) THOMSON & PFLUG46. Tricolpopollenites densus PFLUG in THOMSON & PFLUG47. Quercopollenites robur PLANDEROVÁ48–52. Tricolporopollenites cingulum (R. POTONIÉ) THOMSON & PFLUG53–56,70. Tricolporopollenites megaexactus (R. POTONIÉ) THOMSON & PFLUG57,58. Tricolporopollenites krucshi (R. POTONIÉ) THOMSON & PFLUG ssp. pseudolaesus (R. POTONIÉ) THOMSON & PFLUG59–62. Tricolporopollenites microreticulatus PFLUG & THOMSON in THOMSON & PFLUG63,64. Tricolporopollenites krucshi (R. POTONIÉ) THOMSON & PFLUG ssp. rodderensis THIERGART65. Quercopollenites mongolica PLANDEROVÁ66. Tricolpopollenites retiformis PFLUG & THOMSON in THOMSON & PFLUG67–69. Tricolporopollenites microreticulatus PFLUG & THOMSON in THOMSON & PFLUG71. Tricolporopollenites porasper PFLUG in THOMSON & PFLUG72. Tetracolporopollenites microellipsus PFLUG in THOMSON & PFLUG73. Polycolporopollenites sp.74. Periporopollenites stigmosus (R. POTONIÉ) THOMSON & PFLUG


397

1 23 4 5 6

36

78

9 10

11 12 13 14 15 16

1819

2021

22 23

24

25

26

17

27 2829 30 31

32 33

3435

37 38 39 40 41 42 43

44 4546

4748 49 50 51 52 53 54 55 56

57 58 59 60 61 62

63 64

65

66 6768 69 70

71 7273

74


398

PLATE VI

(EVL‹K)(All illustrations X 500)

Figure 1. Leiotriletes microadriennis W. KRUTZSCH 2. Stereisporites (Stereoides) stereoides (R. POTONIÉ & VENITZ) THOMSON & PFLUG3. Laevigatosporites haardti (R. POTONIÉ & VENITZ) THOMSON & PFLUG 4,6,7. Pityosporites microalatus (R. POTONIÉ) THOMSON & PFLUG 5. Pityosporites libellus (R. POTONIÉ) NAKOMAN8. Pityosporites alatus W.KRUTZSCH9,10. Inaperturopollenites hiatus (R. POTONIÉ) PFLUG & THOMSON in THOMSON & PFLUG11. Inaperturopollenites polyformosus (THIERGART) THOMSON & PFLUG12. Cupressacidites cuspidateaformis (ZAKLINSKAJA) W. KRUTZSCH13,14. Graminidites laevigatus W. KRUTZSCH15. Sparganiapollenites neogenicus W. KRUTZSCH16,17. Cycadopites spp.18,19. Monogemmites pseudosetarius WEYLAND & PFLUG20. Triatriopollenites bituitus (R. POTONIÉ) THOMSON & PFLUG21,22. Momipites punctatus (R. POTONIÉ) NAGY23,24. Triporopollenites simpliformis PFLUG & THOMSON in THOMSON & PFLUG25. Triporopollenites undulatus PFLUG in THOMSON & PFLUG26. Reevesiapollis triangulus (MAMCZAR) W. KRUTZSCH27. Polyvestibulopollenites verus PFLUG in THOMSON & PFLUG28. Subtriporopollenites simplex (R. POTONIÉ & VENITZ) THOMSON & PFLUG 29–30. Intratriporopollenites instructus (R. POTONIÉ) THOMSON & PFLUG31. Intratriporopollenites sp.32. Polyporopollenites undulosus (WOLFF) THOMSON & PFLUG 33. Tricolpopollenites henrici (R. POTONIÉ) THOMSON & PFLUG34. Tricolpopollenites microhenrici (R. POTONIÉ) THOMSON & PFLUG35–37. Quercopollenites robur PLANDEROVÁ38–40. Quercopollenites mongolica PLANDEROVÁ41,42. Tricolpopollenites liblarensis THOMSON & PFLUG43. Tricolpopollenites retiformis PFLUG & THOMSON in THOMSON & PFLUG44–54,70,71.Tricolporopollenites cingulum (R. POTONIÉ) THOMSON & PFLUG 55–61. Tricolporopollenites megaexactus (R. POTONIÉ) THOMSON & PFLUG62,63. Tricolporopollenites pacatus PFLUG in THOMSON & PFLUG64. Tricolporopollenites macrodurensis PFLUG & THOMSON in THOMSON & PFLUG65–69. Tricolporopollenites microreticulatus PFLUG & THOMSON in THOMSON & PFLUG72. Tetracolporopollenites abditus PFLUG in THOMSON & PFLUG73. Tetracolporopollenites microrobustus PFLUG in THOMSON & PFLUG74. Periporopollenites stigmosus (R. POTONIÉ) THOMSON & PFLUG


399

12

3 45 6

7 8

9 1011

12 13 14 15

1618 19 20

21 22 23 24 2526

17

27 28

29 30 3132

3334 35

36 37 38 39 40 41 42 43 44 45

46 47 48 49 50 51 52 53 54 55

56 57 58 5960 61 62 63

6465

66 67 68 69 70 71 72 7374


400

PLATE VII

(‹NCESU-ZAMBAL)(All illustrations X 500)

Figure 1. Leiotriletes microadriennis W. KRUTZSCH 2. Polypodiaceoisporites sp.3. Baculatisporites primarium (WOLLF) THOMSON & PFLUG4. Levigatosporites haardti (R. POTONIÉ & VENITZ) THOMSON & PFLUG5–7. Pityosporites strobipites (WODEHOUSE) W. KRUTZSCH8. Pityosporites alatus W. KRUTZSCH9. Pityosporites libellus (R. POTONIÉ) NAKOMAN 10,11. Inaperturopollenites hiatus (R. POTONIÉ) PFLUG & THOMSON in THOMSON & PFLUG12,13. Inaperturopollenites polyformosus (THIERGART) THOMSON & PFLUG14. Ephedripites sp.15. Graminidites laevigatus W. KRUTZSCH16. Graminidites subtiliglobosus W. KRUTZSCH17. Cycadopites sp.18. Iteapollis angustiporatus (SCHNEIDER) ZIEMBINSKA–TWORZYDLO19. Sparganiapollenites neogenicus W. KRUTZSCH20. Monogemmites pseudosetarius WEYLAND & PFLUG21–23. Triatriopollenites bituitus (R. POTONIÉ) THOMSON & PFLUG24. Triatriopollenites corypheause (R. POTONIÉ) THOMSON & PFLUG25,26. Momipites punctatus (R. POTONIÉ) NAGY27. Triporopollenites coryloides PFLUG in THOMSON & PFLUG28. Rhamnaceaepollenites triquetrus THIELLE–PFEIFFER29–31. Polyvestibulopollenites verus PFLUG in THOMSON & PFLUG32,33. Subtriporopollenites simplex (R. POTONIÉ & VENITZ) THOMSON & PFLUG34. Subtriporopollenites sp.35. Corsinipollenites occulis ssp. noctis (THIERGART) NAKOMAN36,37. Polyporopollenites undulosus (WOLFF) THOMSON & PFLUG 38. Polyporopollenites stellatus (R. POTONIÉ & VENITZ) THOMSON & PFLUG39,40. Polyporopollenites carpinoides PFLUG & THOMSON in THOMSON & PFLUG41. Porocolpopollenites sp.42,43. Tricolpopollenites henrici (R. POTONIÉ) THOMSON & PFLUG44. Tricolpopollenites densus PFLUG in THOMSON & PFLUG45–50. Tricolpopollenites microhenrici (R. POTONIÉ) THOMSON & PFLUG51–54. Tricolporopollenites megaexactus (R. POTONIÉ) THOMSON & PFLUG55. Tricolporopollenites euphorii (R. POTONIÉ) THOMSON & PFLUG 56. Tricolporopollenites krucshi (R. POTONIÉ) THOMSON & PFLUG ssp. rodderensis THIERGART57,58. Tricolporopollenites iliacus (R. POTONIÉ) n.comb. THOMSON & PFLUG59,60. Periporopollenites multiporatus PFLUG in THOMSON & PFLUG61. Periporopollenites stigmosus (R. POTONIÉ) THOMSON & PFLUG


401

1 2 3 4 5 6

36

7 8

9 10 11

12 1314

1516

1819

2021 22

2324 25 26

17

27 28

29 3031 32 33 34

35

37 38 39 4041

42 43

44 45 46 47 48 49 50 51 52 53

5455

5657 58

59 6061


402

PLATE VIII

(VASILTEPE)(All illustrations X 500)

Figure 1. Stereisporites involutus W. KRUTZSCH ssp. minutoides W. KRUTZSCH2. Polypodiaceoisporites sp.3. Laevigatosporites haardti (R. POTONIÉ & VENITZ) THOMSON & PFLUG4,5. Pityosporites microalatus (R. POTONIÉ) THOMSON & PFLUG6. Pityosporites strobipites (WODEHOUSE) W. KRUTZSCH7. Inaperturopollenites dubius (R. POTONIÉ & VENITZ) PFLUG & THOMSON in THOMSON & PFLUG8,9. Inaperturopollenites verrupapillatus TREVISAN10,11. Inaperturopollenites polyformosus (THIERGART) THOMSON & PFLUG12,13. Ephedripites spp.14,15. Monoporopollenites gramineoides MEYER16. Graminidites subtiliglobosus W. KRUTZSCH17,18. Graminidites sp.19. Sparganiapollenites neogenicus W. KRUTZSCH20,21. Cycadopites spp.22,23. Monogemmites pseudosetarius WEYLAND & PFLUG24,25. Iteapollis angustiporatus (SCHNEIDER) ZIEMBINSKA–TWORZYDLO26–29. Triatriopollenites rurensis PFLUG & THOMSON in THOMSON & PFLUG30–33. Triatriopollenites myricoides (KREMP) THOMSON & PFLUG34,35. Triatriopollenites bituitus (R. POTONIÉ) THOMSON & PFLUG36. Triatriopollenites coryphaeuse (R. POTONIÉ) THOMSON & PFLUG37. Momipites punctatus (R. POTONIÉ) NAGY38–41. Platycarya miocaenicus NAGY42. Triporopollenites simpliformis PFLUG & THOMSON in THOMSON & PFLUG43. Triporopollenites labraferus (R. POTONIÉ) THOMSON & PFLUG44. Triporopollenites coryloides PFLUG in THOMSON & PFLUG45. Reevesiapollis triangulus (MAMCZAR) W. KRUTZSCH46,47. Intratriporopollenites instructus (R. POTONIÉ) THOMSON & PFLUG48,49. Subtriporopollenites simplex (R. POTONIÉ & VENITZ) THOMSON & PFLUG50. Polyporopollenites undulosus (WOLFF) THOMSON & PFLUG51–55. Myrtaceidites mesonesus COOKSON & PIKE56,57. Tricolpopollenites microhenrici (R. POTONIÉ) THOMSON & PFLUG58,60. Quercopollenites robur PLANDEROVÁ61. Tricolpopollenites retiformis PFLUG & THOMSON in THOMSON & PFLUG62. Tricolpopollenites sp.63. Tricolporopollenites cingulum (R. POTONIÉ) THOMSON & PFLUG64,65. Tricolporopollenites microreticulatus PFLUG & THOMSON in THOMSON & PFLUG66. Tricolporopollenites pacatus PFLUG in THOMSON & PFLUG67–71. Tricolporopollenites sp. (Asteraceae–Tubulifloreae type)72,73. Tricolporopollenites sp. (Cichorieae- Ligulifloreae type)74. Tetracolporopollenites abditus PFLUG in THOMSON & PFLUG75. Tetracolporopollenites microrobustus PFLUG in THOMSON & PFLUG76. Polycolporopollenites sp.77–80. Periporopollenites halifani NAKOMAN 81–84. Tricolporopollenites sp. (Geraniceae type)


403

1 2 34 5

6

36

7

8 9 10 11 12 13

14

15

16

18

19 20 21 23 24 2526

17

27 28

29 31 32 33 34 35 37 38

39

40

41

42 43 44 45 46 47 4849

50 5152

53

54

55

56 57 58 59 6061 62

63 6465 66 67

68 69 70 71

7273

74

22

30

7576 77 78 79 80

81 8283 84

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