2018 | 71/3 | 121 – 133 | 14 Figs. | 3 Tabs. | www.geologia-croatica.hr Journal of the Croatian Geological Survey and the Croatian Geological Society 1. INTRODUCTION The Cretaceous to Neogene marine successions are in the north- ern, western and eastern parts of the Isparta Angle. Within the context of the regional stratigraphy, sedimentology and tectonic evolution, many studies were carried out by GUTNIC et al. (1979), KARAMAN (1990, 1994), YAĞMURLU (1994), ŞENEL (1997), GÖRMÜŞ & ÖZKUL (1995), GÖRMÜŞ et al. (2001, 2004), POISSON et al. (2003) and ROBERTSON et al. (2003). There are problems concerning the geological mapping, age of sedimenta- tion and environmental interpretation of Palaeogene and Neogene sediments in the region. In previous studies the marine clastics and the carbonate rock series of the studied area were mainly de- scribed as Eocene flysch by GUTNIC et al. (1979), the Kayıköy Formation (Eocene) by YAĞMURLU (1994), Isparta flysch (Eo- cene) by GÖRMÜŞ & ÖZKUL (1995), the Elmalı Formation (Lu- tetian to Burdigalian) by ŞENEL (1997) and Yavuz Flysch (Eo- cene) by POISSON et al. (2003). Clastic and carbonaceous deposits, belonging to the Güneyce Formation in the studied area, were interpreted by BARRIER & VRIELYNCK (2008) as the Derinçay Formation corresponding to platform or shallow shelf carbonate or terrigenous clastics, deposited at the back-arc basin or on the low-land margin of the active subduction zone placed in the Eastern Mediterranean Basin. The scope of the study is to provide new biostratigraphic data from the sediments of the Isparta and the Güneyce formations for the new geologic map. The proposed new Lower Miocene marine clastics of the Güneyce Formation, which extend in the northern part of the Isparta Angle, are significant for the Eastern Mediterranean geology. 2. GEOLOGICAL SETTING There are two different geological interpretations on the stratig- raphy of the Palaeogene and Neogene marine sequences and their Revised chrono-biostratigraphy of Lower Miocene deposits of the Eastern Mediterranean (SW Turkey), based on calcareous nannofossils Gülin Yavuzlar* and Enis Kemal Sagular Suleyman Demirel University, Faculty of Engineering, Departament of Geological Engineering, West Campus, Cunur, TR32260 Isparta, Turkey; (corresponding author: gulinyavuzlar@gmail.com*, eniskemal@gmail.com) doi: 10.4154/gc.2018.15 Abstract Lower Miocene deposits of the Güneyce Formation formerly described as the Elmalı Formation of Lutetian-Burdigalian age are located near the villages of Gökçebağ (Burdur) and Yakaören (Ispar- ta), (southwestern Turkey), Eastern Mediterranean, and overlie the pre-Neogene tectonostrati- graphic units of the Isparta Angle. The purpose of this study is to discuss new biostratigraphic da- ta calibrated to originally classified nannofossil records. Three Early Miocene nannofossil biozones, NN1 - Triquetrorhabdulus carinatus Zone, NN2 - Discoaster druggii Zone and NN3 – Sphenolithus belemnos Zone, were defined in clastic sediments of the Güneyce Formation. In addition, one Lu- tetian biozone, NP16 – Discoaster tanii nodifer Zone, was recognized in the remaining outcrops of the Isparta Formation unconformably underlying the Güneyce Formation. Nannofossil assemblages of shallow marine deposits in the Güneyce Formation contain high amounts of reworked (Palaeogene and Cretaceous) specimens. New biostratigraphic data and sedimentary features of the Güneyce Formation clastics indicate shallow marine deposition and the beginning of the transgression, spreading over an erosional surface on the ophiolitic melange and Cretaceous to Eocene marine successions rising to the west of the region. structural constructions related to the study area. The accepted former (and common) view is that the Eocene marine sedimen- tary successions (Elmalı Formation) were overthrust by the ophi- olitic melange (Gökçebağ Melange) after the Early Miocene (Fig. 1). However, the results of this study show that there are two an- gular unconformable marine successions, the Isparta Formation (Lutetian) and the Güneyce Formation (Early Miocene), overlying the ophiolitic melange (Fig. 2). In the region, the Yavuz Flysch (GUTNIC et al., 1979), was described as marine carbonate and clastics deposited during the Paleocene to Eocene (Lutetian in- terval) and the second succession, the Elmalı Formation (ŞENEL, 1997), was described as marine shelf clastics deposited during the Lutetian or ranging from the Lutetian to the Burdigalian. Accord- ing to GÖRMÜŞ et al. (2001), the studied Güneyce Formation comprises six lithological units from the bottom to the top: (1) mudstone dominated facies (muddy facies); (2) sandstone domi- nated facies (sandy facies); (3) olistostrome facies; (4a) rhythmic sandstone-mudstone facies; (4b) carbonate facies; (5) sandstone facies and (6) coarse clastics-conglomerates facies. In this area, there are particularly clastic facies 1 to 4a. The overlying units of the investigated area are Plio-Quaternary volcanics and Quater- nary alluvium or colluvial fan deposits. 3. MATERIAL AND METHODS In this study, 35 samples of various grain-sized clastic or carbon- ate rocks such as marls, mudstones, sandstones or limestones were collected and examined from 17 locations within the three measured stratigraphic sections. All the study material obtained from YAVUZLAR (2015) is preserved in the General Geology Laboratory of Suleyman Demirel University. The three stratig- raphic sections, Necibin Tepe, Arapdere and Abidinoğlutaşı Tepe were researched in the field (Fig. 3). The sedimentary succession Article history: Manuscript received January 08, 2018 Revised manuscript accepted July 16, 2018 Available online October 17, 2018 Keywords: Aquitanian, Burdigalian, biostratigraphy, calcareous nannofossils, marine deposits, geologic map G eo lo gi a C ro at ic a Geologia Croatica 71/3122 of the Güneyce Formation begins with terrestrial deposits inclu- ding gypsum and coal-bearing sandy-mudstones, and continues with rhythmic sandstone and mudstone/marl alternations inclu- ding sand-dominated levels. Clastic rock packages seen are par- tially similar to the depositional facies 1-4a of GÖRMÜŞ et al. (2001). 3.1. Stratigraphic sections The Necibin Tepe stratigraphic section (Figs. 3 A, 4) belongs to the first sedimentary levels of the Güneyce Formation overlying the ophiolitic melange. In the lower part of the succession (up to 44 m), there are sandy mudstones with sandstone interbeds of sandy facies of the Güneyce Formation, followed by dolomitic limestone lenticular beds within the muddy marine sedimenta- tion. In addition, these levels include lense-shaped gypsum and coal intercalations that could belong to very shallow olistostrome facies. Above sixty metres, there is a shallow marine sandstone and mudstone alternation in the upper part of the succession be- longing to the rhythmic sandstone-mudstone facies of the Güneyce Formation. In the Necibin Tepe section, a transgression Figure 1. A new detailed version of the map, built on the existing geologic maps (GUTNIC et al., 1979, ŞENEL, 1997). Figure 2. A new geologic 3D map was built based on nannofossil biostratigraphy (emended from YAVUZLAR & SAGULAR, 2016). G eologia C roatica Yavuzlar and Sagular: Revised chrono-biostratigraphy of Lower Miocene deposits of the Eastern Mediterranean (SW Turkey) ... 123 Figure 3. Measured stratigraphic sections in the Güneyce Formation: A. Necibin Tepe stratigraphic cross section, B. Arapdere stratigraphic cross section, C. Abidinoğlutaşı Tepe stratigraphic cross section (emended from YAVUZLAR & SAGULAR, 2017). Figure 4. Lithostratigraphy of the Necibin Tepe section. G eo lo gi a C ro at ic a Geologia Croatica 71/3124 resulted in deposition of shallow marine sediments on top of ter- restrial sedimentary rocks and facies of the succession. The Arapdere stratigraphic section (Figs. 3 B, 5) belongs to the middle levels of the Güneyce Formation following the sedi- ments of Necibin Tepe section. Here, sediments and facies of the succession exhibit the rhythmic alternations of mudstones and sandstones representing shallow marine sedimentation. The Abidinoğlutaşı Tepe stratigraphic section (Figs. 3 C, 6) belongs to the rhythmic sandstone-mudstone facies of the Gü- neyce Formation, overlies the ophiolitic melange and coincides with the sediments of the Arapdere section. The sedimentary successions and facies of this section also include mudstone and sandstone rhythmic alternation representing shallow marine se- dimentation. 3.2. Investigation methods The standard nannofossil preparation method was used without applying any concentration or cleaning process and taxonomic Figure 5. Lithostratigraphy of the Arapdere section. Figure 6. Lithostratigraphy of the Abidinoğlutaşı Tepe section. Figure 7. Distribution of original nannofossil percentages in the Necibin Tepe section (* indicates nannofossil data in thin section). G eologia C roatica Yavuzlar and Sagular: Revised chrono-biostratigraphy of Lower Miocene deposits of the Eastern Mediterranean (SW Turkey) ... 125 concepts were followed PERCH-NIELSEN (1985a), BOWN & YOUNG (1998). Analyses were carried out by polarized light mi- croscopes at x2500 magnification, using a Nikon Optiphot-Pol and Leica DM2700 P, at the Department of Geology, Suleyman Demirel University. For each smear slide, nannofossil specimens were counted in 200 fields of view and the identified species were separated into two groups as autochthonous and reworked taxa. In addition, thinned (20-25 microns) petrographic sections were prepared from coarse grained rock samples such as sand- stone and limestone (SAGULAR, 2003a, 2003b). Nannofossil re- cords within lithoclasts or within the matrix in thin-sections of a sandstone are considered to be mainly reworked sedimentary grains. The nannofossils within intraclasts or within the calcite cement of a calcarenite or limestone could be coeval with sedi- mentation (synsedimentary). Nannofossil records observed in lithoclasts are considered as reworked from extrabasin sources whereas those in intraclasts are considered as removed from else- where within the basin. Whereas, fossil data found in matrix or cement are considered either reworked or resedimented. Thus, the autochthonous or reworked nannofossil assemblages and their sedimentological properties were determined in both nannofossil smear-slides and thin-sections. The results of the laboratory de- terminations were correlated with field observations and previous studies. MELINTE (2005), WADE & BOWN (2006) used the nan- nofossil population as an indicator of sea level changes. SAGU- LAR (2003b) described another method based on reworked nan- nofossil data, where the reworked specimen proportions are used as an indicator of sea level changes in coastal environments. The method which SAGULAR (2003b) described is applied in this study. 4. RESULTS 4.1. Nannofossil biostratigraphy Four nannofossil biozones according to MARTINI’s (1971) zona- tion were identified (Fig. 10). 4.1.1. Discoaster tani nodifer Zone (NP16) Definition: The last occurrence (LO) of Rhabdolithus gla- dius to the LO of Chiasmolithus solitus Authors: HAY et al. (1967), emend. MARTINI (1970) Age: Lutetian, Middle Eocene Type locality: The NP16 Zone covers the Isparta Formation observed in only a few outcrops within the investigated area (south of Gökçebağ Village, west of the investigated area, Fig. 2). Remarks on assemblage: The LO of Chiasmolithus solitus in the upper part of the zone and the first occurrence (FO) of Re- ticulofenestra umbilicus and LO Blackites inversus at the base Figure 8. Distribution of original nannofossil percentages in the Arapdere section (*indicates nannofossil data in thin section). Figure 9. Distribution of original nannofossil percentages in the Abidinoğlutaşı Tepe section (* indicates nannofossil data in thin section). G eo lo gi a C ro at ic a Geologia Croatica 71/3126 Figure 10. Biozones and marker nannofossils of the Isparta and the Güneyce formations. Figure 11. Smear slide images of dinoflagellate cysts in sample 14G004B:1A-D) T. heimii and coalized Thoracosphaera spp. (T. heimii ?); 2-4) T. heimii (PL: polarized light, CL: phase contrast, QL: with quartz wedge, GL: with gypsum wedge). G eologia C roatica Yavuzlar and Sagular: Revised chrono-biostratigraphy of Lower Miocene deposits of the Eastern Mediterranean (SW Turkey) ... 127 (BOWN & NEWSAM 2017, PERCH-NIELSEN 1985) is noticed in the assemblage with D. saipanensis, D. tanii nodifer, R. dic- tyoda and S. radians and B. inversus. 4.1.2. Triquetrorhabdulus carinatus Zone (NN1) Definition: LO of Helicosphaera recta and/or Sphenolithus ciperoensis to the FO of Discoaster druggii Authors: BRAMLETTE & WILCOXON (1967), emend. MARTINI & WORSLEY (1970) Age: Aquitanian, Early Miocene Type locality: The base of the Arapdere section Remarks on assemblages: The LO of Cyclicargolithus abi- sectus is observed in the assemblage with T. caritanus, C. flori- danus, Reticulofenestra bisecta, Sphenolithus dissimilis. In this zone, the presence of S. moriformis, S. compactus and T. heimii were observed in samples from the Necibin Tepe section. In the Arapdere section the following species were identified: C. miope- lagicus, C. pelagicus, C. abisectus, C. floridanus, R. bisecta, R. gelida, R. producta, S. compactus, S. dissimilis, S. moriformis and T. carinatus. 4.1.3. Discoaster druggii Zone (NN2) Definition: FO of Discoaster druggii to the LO of Tri- quetrorhabdulus carinatus. Authors: MARTINI & WORSLEY (1970) Age: Aquitanian to Burdigalian, Early Miocene Table 1. List of calcareous nannofossil species distribution, counts and percentages in the Necibin Tepe section (* indicates thin section nannofossil data). SP EC IE S S. c om pa ct us S. m or ifo rm is T. h ei m ii ∑ c oe va l L ow er M io ce ne % a ut oc ht on ou s R. h es sl an di i S. m or ifo rm is T. sa xe a ∑ E oc en e % re w or ke d Eo ce ne M . m ur us W . b ar ne si ae ∑ C re ta ce ou s % re w or ke d C re ta ce ou s Tr iq ue tro rh ab du lu s c ar ita nu s Z on e (N N 1) 14G003A* 1 1 33 1 1 2 67 14G003B 1 1 100 14G003C 1 1 2 4 57 2 2 29 1 1 14 14G004B 50 50 100 14G004C 1 1 50 1 1 50 14G004D 1 1 50 1 1 50 14G004E* STERILE 14G004F 1 1 100 14G002A* STERILE 14G002B STERILE 14G002C STERILE 14G006A STERILE 14G006B* STERILE 14G006C* STERILE Table 2. List of calcareous nannofossil species distribution, counts and percentages in the Arapdere section (* indicates thin section nannofossil data). B IO ZO N E SA M PL ES B. b ig el ow ii C . m io pe la gi cu s C . p el ag ic us C . a bi se ct us C . fl or id an us D . d ru gg ii R. b is ec ta R. g el id a R. h aq ii R. m in ut a R. p ro du ct a S. c om pa ct us S. d is si m ili s S. m or ifo rm is T. h ei m ii T. c ar in at us ∑ c oe va l L ow er M io ce ne % a ut oc ht on ou s B. b ig el ow ii C . e op el ag ic us C . p el ag ic us D . b ar ba di en si s D . k ue pp er i E. o va lis R. h es sl an di i S. m or ifo rm is Z. b iju ga tu s ∑ re w or ke d Eo ce ne % re w or ke d Eo ce ne T. sa xe a ∑ re w or ke d Pa le oc en e % re w or ke d Pa le oc en e M ic ul a sp . M . m ur us M . s ta ur op ho ra ∑ re w or ke d C re ta ce ou s % re w or ke d C re ta ce ou s N N 3 14K007 2 6 2 10 62 2 2 14 4 4 25 BI003A 1 2 4 2 4 13 38 1 14 4 2 21 62 BI003B* 1 2 3 100 14K006 2 2 2 2 1 1 10 100 14K004 2 2 6 2 4 2 6 24 75 2 2 2 6 19 2 2 6 14K005 12 6 15 8 5 2 22 70 97 2 2 3 N N 2 BI001A* 2 1 1 1 9 14 93 1 1 7 BI001B 1 1 2 67 1 1 33 BI001C 1 1 1 1 1 3 1 1 3 13 87 1 1 2 13 N N 1 14K001A 2 6 3 12 18 2 6 2 11 16 2 80 100 14K001B 2 2 2 1 7 58 2 2 1 5 42 G eo lo gi a C ro at ic a Geologia Croatica 71/3128 Type locality: Arapdere section Remarks on assemblages: Discoaster druggii, Reticulofen- estra haqii, Coccolithus miopelagicus and Sphenolithus mori- formis are present. Apart from the samples of the measured sec- tion, Triquetrorhabdulus challengeri were identified in the mudstone spot sample BI016D. 4.1.4. Sphenolithus belemnos Zone (NN3) Definition: LO of Triquetrorhabdulus carinatus to LO of Sphenolithus belemnos Authors: BRAMLETTE & WILCOXON (1967) Age: Burdigalian, Early Miocene Type locality: Arapdere section and Abidinoğlutaşı Tepe section Remarks on assemblages: Sphenolithus belemnos, S. dis- belemnos, S. compactus and S. conicus are considered as marker species in this zone. 4.2. Assemblage composition 4.2.1. Necibin Tepe section In this section fourteen samples were studied and half of them were sterile. The following species were identified: Sphenolithus Figure 12. Thin section images with reworked nannofossil taxa in the matrix of sandstones 1-4) R. hesslandii, (Arapdere section, sample BI001A) 5-6) S. moriformis, (Arapdere section, sample BI001A), 7-8) C. pelagicus (Arapdere section, sample BI001A), 9-10) C. floridanus (Abidinoğlutaşı Tepe section, sample 14G0013A) (PL: polarized light, CL: phase contrast, QL: with quartz wedge, GL: with gypsum wedge). G eologia C roatica Yavuzlar and Sagular: Revised chrono-biostratigraphy of Lower Miocene deposits of the Eastern Mediterranean (SW Turkey) ... 129 compactus, S. moriformis and Thoracosphaera heimii. Almost half of the assemblage contains reworked specimens from the Eocene: Reticulofenestra hesslandii, T. saxea and from the Cre- taceous: Micula murus and Watznaueria barnesiae (Table 1). Above 60 m in the section, deposits turn to the 4a rhythmic sandstone-mudstone facies of the Güneyce Formation defined in calcareous nannofossil NN1, NN2 and NN3 zones at the Arapdere section. Below 60 m in the section, sediments contain only very sparse Miocene Sphenolithus compactus, the first appearance of which is also observed in the NN1 Zone (PERCH-NIELSEN (1985) and AUBRY (1989)) in the autochthonous nannofossil as- semblage with 33 to 67% reworked nannofossils from the Creta- ceous and 33 – 100% from the Lutetian (Fig. 7). This section is very close to the Arapdere section (Fig. 2) and it is positioned at the base of the Arapdere section. 4.2.2. Arapdere section From a total of eleven samples, two were thin-sections and con- tain reworked nannofossil taxa. These samples contain: Braaru- dosphaera bigelowii, Coccolithus miopelagicus, C. pelagicus, Cyclicargolithus abisectus, C. floridanus, Discoaster druggii, Reticulofenestra bisecta, R. gelida, R. haqii, R. minuta, R. pro- ducta, S. compactus, S. dissimilis, S. moriformis, T. heimii and T. carinatus. The reworked assemblage from the Eocene contains: B. bigelowii, C. eopelagicus, C. pelagicus, Discoaster barbadi- ensis, D. kuepperi, E. ovalis, R. hesslandii, S. moriformis, Z. bi- jugatus. T. saxea is determined as reworked from the Paleocene. The reworked Cretaceous nannofossils are Micula sp., M. murus and M. staurophora (Table 2). In the samples of the Arapdere section, the NN1 zone con- tains 28% autochthonous and 72% reworked nannofossils. The NN2 zone contains from 50 to 60% autochthonous and 40 to 50% reworked forms. The NN3 zone includes 58 to 98% autochthonous forms and between 2 and 42% reworked nannofossil taxa (Fig. 8). 4.2.3. Abidinoğlutaşı Tepe section Of nine samples studied, five were thin sections and two were sterile smear slides. The autochthonous species are C. miopelag- icus, C. pelagicus, C. floridanus, D. druggii, R. bisecta, R. haqii, Sphenolithus belemnos, S. disbelemnos, S. compactus, S. conicus, S. dissimilis, S. moriformis, T.heimii. The reworked species are as follows from the Eocene: Chiasmolithus solitus, Coccolithus formosus, C. pelagicus, Discoaster lodoensis, D. mohleri, D. saipanensis, Ericsonia robusta, E. subpertusa, Pyrocyclus inver- sus, Reticulofenestra dictyoda, S. moriformis, S. radians, S. spi- niger and Z. bijugatus. Paleocene taxa include: T. saxea and from the Cretaceous, the following were determined: Calculites ob- scurus, Lucianorhabdus cayeuxii, M. murus, M. staurophora and Watznaueria barnesiae. In samples 14G017B, 14G018B and 14G016B ascidian spicules were observed (Table 3). The autochthonous species belonging to the NN3 zone dis- play percentages from 50 to 73% and reworked species comprise 27 to 50% of the assemblage (Fig. 9). 5. DISCUSSION 5.1. Biostratigraphy and palaeoecology Previous studies in this region were undertaken by GÖRMÜŞ et al. (2001) who first identified the NN1 and NN2 zones. The NN1 Zone was defined by the presence of: C. floridanus, C. abisectus, C. pelagicus, Discoaster deflandrei, D. bisectus, Helicosphaera obliqua, S. conicus, S. compactus, S. dissimilis and Z. bijugatus. The NN2 Zone was defined by the presence of Discoaster drug-Ta bl e 3. L ist o f c al ca re ou s n an no fo ss il sp ec ie s d ist rib ut io n, c ou nt s a nd p er ce nt ag es in th e Ab id in oğ lu ta şı Te pe se ct io n (* in di ca te s t hi n se ct io n na nn of os sil d at a) . BIOZONE SPECIES C. miopelagicus C. pelagicus C. abisectus C. floridanus D. druggii R. bisecta R. haqii S. belemnos S. disbelemnos S. conicus S. compactus S. dissimilis S. moriformis T. heimii ∑ coeval Lower Miocene % autochtonous C. solitus C. formosus C. pelagicus D. lodoensis D. mohleri D. saipanensis E. robusta E. cf. subpertusa P. inversus R. dictyoda S. moriformis S. radians S. spiniger Z. bijugatus ∑ reworked Eocene % reworked Eocene T. saxea ∑ reworked Paleocene % reworked Paleocene C. obscurus L. cayeuxii M. murus M. staurophora W. barnesiae ∑ reworked Cretaceous % reworked Cretaceous Ascidian spicule NN314 G 01 7A * ST ER IL E 14 G 01 7B 1 12 3 1 5 18 1 1 1 11 6 60 76 4 5 3 3 2 2 3 18 23 1 1 1 5 14 G 01 8A * ST ER IL E 14 G 01 8B 3 6 3 3 3 3 8 5 5 39 59 3 8 3 3 3 1 21 29 3 5 8 12 3 14 G 01 3A * 1 3 4 44 5 5 56 14 G 01 3B 24 64 32 40 1 1 1 9 10 84 26 6 80 3 16 10 20 16 65 20 1 1 0 14 G 01 3C * 1 1 10 0 14 G 01 6A 3 8 11 44 1 1 4 13 13 52 14 G 01 6B * 1 1 8 3 1 1 4 9 76 1 1 8 1 1 8 1 G eo lo gi a C ro at ic a Geologia Croatica 71/3130 gii, D. deflandrei, C. floridanus, C. abisectus, Calcidiscus sp, and S. dissimilis. These zones are very diverse and were determined in relatively deeper marine environments than presented here. In this region, the NN3 zone was first described by HEPDENİZ & SAGULAR (2009), defined by the presence of Triquetrorhabdulus carinatus, Discoaster cf. druggii, Sphenoli- thus belemnos, Dictyococcites perplexus, Pyrocyclus cf. oran- gensis, Reticulofenestra haqii, Sphenolithus compactus, Spheno- lithus conicus, Coccolithus miopelagicus. A general distinction of autochthonous and reworked nan- nofossil taxa allows the definition of depositional and paleoenvi- ronmental characteristics and leads to more reliable sedimentary and stratigraphic interpretations, especially for a fluctuating and unfavourable coastal environment (SAGULAR, 2003a, b). In this type of environment, marine deposits, such as the Güneyce For- mation, generally contain very low amounts of autochthonous nannofossil assemblages. Reworked nannofossil assemblages are predominant in the sediments of the Güneyce Formation (Tables 1, 2 and 3). While autochthonous nannofossils display percent- ages between 33 and 100%, the reworked taxa account for be- tween 6 and 100% of the assemblage composition. Based on the generally very high percentages of reworked taxa in the assem- blages the Güneyce Formation can be interpreted as representing a very shallow marine environment (Figs. 7, 8 and 9). The calcareous nannofossil assemblages of the Güneyce For- mation, are dominated by the Sphenolithus genus, as being more common in lower latitudes, preferring warm and shallow waters than open ocean (PERCH–NIELSEN 1985b). According to WEI Figure 13. Thin section images of sandstones with reworked nannofossil taxa 1-2) C. solitus in lithoclast (Abidinoğlutaşı Tepe section, sample 14G0013A), 3-4) R. hesslandii in matrix (Necibin Tepe section, sample 14G003A); 5-8) C. pelagicus in matrix, and 5-7 & 9) C. pelagicus in matrix (Abidinoğlutaşı Tepe section, sample 14G013A) (PL: polarized light, CL: phase contrast, QL: with quartz wedge, GL: with gypsum wedge). G eologia C roatica Yavuzlar and Sagular: Revised chrono-biostratigraphy of Lower Miocene deposits of the Eastern Mediterranean (SW Turkey) ... 131 Figure 14. Thin section images of sedimentary structures in sandstone sample 14G0016B of the Abidinoğlutaşı Tepe section 1) General view of the sandstone, 2-3) Isopachous rim cement and ascidian spicule enclosed in intergranular sparry calcite cement of an intertidal sandstone, 4-6) Neomorphic fibrous fine crystalline spherulite FLÜGEL (1982). G eo lo gi a C ro at ic a Geologia Croatica 71/3132 & WISE (1990) sphenolith diversity is higher in equatorial sites, being less diverse in the mid-latitude areas. Only S. moriformis existed in the high-latitude sites. Within the whole asemblage, 150 individuals were counted and S. moriformis is presented here as the most abundant species. Based on the work of the afore- mentioned authors Sphenolithus spp. abundance and diversity indicate a shallow marine environment of the mid-latitudes. 5.2. Necibin Tepe section The clastic levels in approximately the first 44 m of the section have no nannofossil data due to a prevailing terrestrial or shore- line environment (Figure 4, Table 1). From 44 m - 60 m, the pres- ence of gypsum and microalgal (derived from dinoflagellate cysts) sapropelic coal lenses can be observed in the muddy levels of the succession. Due to the presence of such coal (Fig. 11) and gypsum lenses in the samples of the Necibin Tepe section, it is considered that the Early Miocene sedimentation was started in terrestrial and continued to occur in a littoral environment (Fig. 7). Besides, nannofossil data indicate the NN1 biozone, this sec- tion includes the beginning of the Early Miocene sedimentation of the Güneyce Formation. 5.3. Arapdere section Depending on the original distribution of nannofossil assem- blages within the Miocene to Cretaceous (Table 2), the Arapdere section represents transgressive shallow marine sediment levels in the Güneyce Formation. They include beach sediments or shoreline sandstones representing shallow marine environments such as littoral, tidal or the offshore-transitional zone or clastic shelf and contain mudstones with low coeval nannofossil con- tents. The distribution of autochthonous and reworked nannofos- sils in rock samples indicate sea level fluctuations in the Early Miocene shoreline transgression (Figs. 8 and 12). 5.4. Abidinoğlutaşı Tepe section According to the nannofosil records of the Abidinoğlutaşı Tepe section, autochthonous nannofossil species decrease from the bot- tom levels and then become dominant again in the upper parts of the section (Fig. 9, Table 3). The interpretation of this section is that the sediments of these levels represent shallow marine depo- sitional environments. Additionally, the presence of ascidian spic- ules in the samples 14G017B, 14G018B and 14G016B (Table 3) can be considered as an indicator of a shallow environment (VAN NAME, 1945). From the bottom to the top of the section, the trans- gressive character and sea level fluctuations continue throughout. The proportions of autochthonous and reworked nannofossil as- semblages in the samples of the Abidinoğlutaşı Tepe section indi- cate a generally transgressive trend with unstable sea level change observed in a very shallow coastal environment during the Bur- digalian after the beginning of the Miocene (Figs. 9, 13 and 14). Based on the new results, in addition to previous studies in the southern part of Isparta (GÖRMÜŞ et al., 2001; HEPDENİZ & SAGULAR, 2009), the marine carbonate and clastics of the Isparta Formation were deposited during the Lutetian and the shallow marine shelf clastics of the Güneyce Formation were de- posited during the Lower Miocene. 6. CONCLUSIONS The following nannofossil biozones are represented in this study: the NP16 - Discoaster tanii nodifer Zone, which was defined in the Isparta Formation and three zones in the Lower Miocene: the NN1 - Triquetrorhabdulus carinatus Zone, NN2 - Discoaster druggii Zone and NN3 - Sphenolithus belemnos Zone in the Güneyce Formation. Based on the high amount of reworked nan- nofossil species the Güneyce Formation was probably deposited in a shallow marine environment. The map of the study area was refined and two marine clas- tic sedimentary units were revised and described (the Isparta and Güneyce Formations). An Ophiolitic melange (Gökçebağ mel- ange) was illustrated in regional maps in former studies as hav- ing been thrust over all the sedimentary sequence, in this study the map is modified according to the presented results. Marine clastic sediments unconformably overlie the ophiolitic melange. In addition, the 3D geologic map of the study area is revised and presented here. 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LIST OF CALCAREOUS NANNOFOSSIL TAXA Miocene Nannofossil Taxa: Coccolithus miopelagicus BUKRY Cyclicargolithus abisectus (MÜLLER) WISE Cyclicargolithus floridanus (ROTH & HAY) BUKRY Discoaster druggii BRAMLETTE & WILCOXON Reticulofenestra bisecta (HAY, MOHLER & WADE) ROTH Reticulofenestra haqii BACKMAN Reticulofenestra minuta ROTH Reticulofenestra producta (KAMPTNER) WEI & THIERSTEIN Reticulofenestra pseudoumbilicus (GARTNER) GARTNER Sphenolithus belemnos BRAMLETTE & WILCOXON Sphenolithus compactus BACKMAN Sphenolithus conicus BUKRY Sphenolithus disbelemnos FORNACIARI & RIO Sphenolithus dissimilis BUKRY & PERCIVAL Sphenolithus moriformis (BRONNIMANN & STRADNER) BRAMLETTE & WILCOXON Thoracosphaera heimii (LOHMANN) KAMPTNER Triquetrorhabdulus carinatus MARTINI Triquetrorhabdulus challengeri PERCH-NIELSEN Palaeogene Nannofossil Taxa: Blackites inversus (BUKRY & BRAMLETTE) BOWN & NEWSAM Chiasmolithus gigas (BRAMLETTE & SULLIVAN) RADOM- SKI Chiasmolithus solitus (BRAMLETTE AND SULLIVAN) LOCKER Coccolithus eopelagicus (BRAMLETTE & RIEDEL) BRAM- LETTE & SULLIVAN Coccolithus formosus (KAMPTNER) WISE Coccolithus pelagicus (WALLICH) SCHILLER Discoaster barbadiensis TAN Discoaster deflandrei BRAMLETTE & RIEDEL Discoaster kuepperi STRADNER Discoaster lodoensis BRAMLETTE & RIEDEL Discoaster mohleri BRAMLETTE & PERCIVAL Ericsonia robusta (BRAMLETTE & SULLIVAN) EDWARDS & PERCH-NIELSEN Discoaster saipanensis BRAMLETTE & RIEDEL Ericsonia subpertusa HAY & MOHLER Reticulofenestra dictyoda (DEFLANDRE IN DEFLANDRE & FERT) STRADNER Reticulofenestra gelida (GEITZENAUER) BACKMAN Reticulofenestra hesslandii (HAQ) ROTH Sphenolithus moriformis (BRONNIMANN & STRADNER) BRAMLETTE & WILCOXON Sphenolithus radians DEFLANDRE Sphenolithus spiniger BUKRY Thoracosphaera heimii (LOHMANN) KAMPTNER Thoracosphaera saxea STRADNER Zygrhablithus bijugatus (DEFLANDRE) DEFLANDRE Mesozoic Nannofossil Taxa: Calculites obscurus (DEFLANDRE) PRINS & SISSINGH IN SISSINGH Lucianorhabdus cayeuxii DEFLANDRE Micula VEKSHINA Micula murus (MARTINI) BUKRY Micula staurophora (GARDET) STRADNER Thoracosphaera heimii (LOHMANN) KAMPTNER Watznaueria barnesiae (BLACK) PERCH-NIELSEN