A GEOLOGICAL STUDY IN THE PENINSULA

Adnan KALAFATÇIOĞLU

Mineral Research and Exploration Institute of

ABSTRACT. — The oldest formations in the Karaburun Peninsula exposed to the effects of the Hersinian and Alpine orogenies, are conglomerates, graywackes, arkoses, sandstones, schists, quartzites and limestones. Lack of fossils in the Devonian system made it impossible to go into distinguishing further subdivisions. Lower Carboniferous limestones containing fossils overlie De- vonian series. Unlike in Sakız Island, where unconformities are occasionally observed, such is not the case in the Karaburun Peninsula. The Mesozoic starts by a conglomerate base laid upon the Paleozoic formations and as a rule contains sandstones and limestones. Although a few Upper Triassic fossils are encountered in it, the well-defined ones belong to the Jurassic system. Jurassic-Lower Cretaceous-Upper Cretaceous ensemble (including Turonian) presents a com- prehensive series in the form of massive and plated limestones. The Upper Cretaceous (Maestrich- tian) overlying this series also begins with a basal conglomerate and comprises pink limestones and sandstones overlain by grey and white compact schistose limestones showing good stratifica- tion. The youngest fossiliferous sediments in this area belong to the Miocene. Miocene systems composed of sandstones, clay, marls and limestones with intercalated tuff show that volcanism was on during the Neogene. In the course of this period rhyolitic, andesitic and basaltic lavas escaping from the cracks came up to cover older formations and a multitude of such cracks and faults came to be as a resultr of volcanic activities. After this introduction, the following may be pointed out regarding the local paleogeography and tectonic history. Paleozoic formations which came up above sea level due to the Hersinian folding went down again during the Upper Triassic (possibly Jurassic) and the sea lasted till the end of the Turonian epoch. Then in the course of the sub-Hersinian phase the area emerged from under the sea but transgressions in the Maestrichtian time caused it to sink once more below the sea level. The upper layers of the Maestrichtian show strong folding and small synclines and anticlines, indicating that the Alpine orogeny took place during the Late Cretaceous or some- what later and the Maestrichtian limestones were severely folded while they were not yet completely solidified. Folding, during the Mesozoic time, did not occur under unidirectional forces. Here, rather a set of multidirectional movements are observed. The Neogene sediments overlie older formations beginning with a red layer of conglomerate at the bottom. In the eastern part of our district there exists a basal conglomerate between Mio- cene and Pliocene formations.

I. INTRODUCTION km away from Izmir and only 15 km The area under study is the 60 km from the Island of Sakız. Examination long Karaburun Peninsula and the vi- of rock samples and subsequent determi- cinity, extending N-S in the Western nations were taken up by Dr. P. de , west of the vilayet of İzmir. Wijkerslooth, Dr. C. Kieft and Dr. Klaus The work was conducted to cover a Markus. Fossils were identified by Miss total of 1600 square kilometres, equally Sevinç Başad, Dr. C. Öztemür and Dr. divided between the map-sections No. Y. Ginkel. I feel indebted and owe many 86/1 and 86/3. The area is roughly 50 thanks to the gentlemen cited above, A GEOLOGICAL STUDY IN THE KARABURUN PENINSULA 41

and also to Dr. Cahit Erentöz for valu- able suggestions and to Prof Dr. İhsan Ketin who helped me during my field work.

II. GEOGRAPHY Although not much elevated, this district, with its suddenly rising hills right along the shore line, gives the im- pression of a mountainous country. In the Peninsula, surrounded by plains at sea level and tectonic troughs, there are valleys encircled by mountains of lime- stones and andesites. Highest peaks are Akdağ (1212 m), Bölmece (848 m) and Kırdağ (707 m).

While the northern part is dotted III. PREVIOUS STUDIES with hills, the Çeşme depression area forms a flat stretch of land. Morpholo- In 1911, A. Philippson (8) carried gically four groups may be distinguished out the geologic survey of the entire in the district : a) Devonian sandstones Peninsula, drew a geologic map of it and limestones, b) Mesozoic limestones, and correlated formations there with c) Neogene sediments and d) andesites those of and the Island of Sakız. and basalts. Here we find high cliffs of According to Phillippson, limestone for- the Alpine character, difficult to cross, mations covering the higher parts as in the Mesozoic limestones, as well as well as wide flat are of Mesozoic age deep dry valleys and the like, in eroded and represented in two fades : a) the limestone formations. Vast area of the massive limestone facies and b) the Devonian age lying to the NW of the plated limestone facies, corresponding district has a monoclinal structure dip- ping west. The morphological structure to the Olonese limestones in Greece is built of Neogene sediments and tuffs. (they contain secondary intercalated In some places andesites form individu- schists). al hills void of vegetation. The area is In 1921 Ktenas conducted a survey usually dry during the summer and wet in northern section of the Peninsula to during the winter. It is drained mainly by streams of water such as Örendere, find the eastwardly continuation of the Söğütdere flowing due south and due formations in Sakız and pointed out the north and their tributaries. following groups of the Paleozoic : 42 Adnan KALAFATÇIOĞLU

In 1939 Werner Paeckelmann (7) set outcrop in the northwestern part of the age of the limestones in the region the map-section 86/1 over a stretch of of Çeşme as being Triassic. area 20 km long and 10 km wide, con- Nuriye Pınar mentioned the exist- sisting mainly of schist, sandstone, arkose, enee of a great number of hot springs conglomerate, graywacke, quartzite and and mineral water sources within the grey limestone layers imbedded in schists depression area of Çeşme. and graywackes. This series is subdivided Mehmet Akartuna (1) claims that into several groups by Ktenas, ranging there is a discordance visible between up to the Upper Carboniferous. We the Miocene and Pliocene formations think this series should best be consider- just east of the Peninsula. ed of the Devonian age, without going into further subdividing. Because, inclu- IV. STRATIGRAPHY ded into the Middle and Upper Carbon- iferous, it underlies the fossiliferous A. Paleozoic Lower Cretaceous limestones, indicating Devonian. — Devonian formations continuous sedimentation. A GEOLOGICAL STUDY IN THE KARABURUN PENINSULA 43

Within this series, roughly 3000 m Middle Carboniferous, showing angular thick, neither fossils nor any sedimen- unconformity. While, to the south of tation gaps are encountered. Its relation Yelkentaş, in the Peninsula of Karabu- to the other Devonian formations may run graywackes and schists of the De- be summarized as follows : Although vonian age underlie Lower Carbonife- the under part of the Devonian sedi- rous limestone with fossils and without ments is not visible in the district, it is any sign of unconformity. At a typical a known fact that the semi-metamorphic section in the region of Örendere, of series of pre-Devonian age outcropping the northern part of the map-section in the Island of Spalmatori, to the west 86/1, is seen a basal conglomerate of of the Peninsula, here constitutes the the Mesozoic age overlying the Devonian lower parts of the Devonian deposition. series. Limestone banks are encountered The relation of this latter with the Lo- in the upper parts of this Devonian wer Carboniferous limestones overlying series and here, most probably, lime- it is not very clearly indicated. In the stones and sandstones grade into one Island of Sakız Devonian is overlain by another. Limestones estimated to belong 44 Adnan KALAFATÇIOĞLU to the Lower Carboniferous seem to be Glomospira eroded out and presently non existent. Tolypammina Whereas, a little to the south, portions Trepeilopsis of the limestones that escaped complete Hyperammina erosion are still visible. Globivalvulina Palaeotextularia Lower Carboniferous-— The grey, Endothyra compact, crystalline limestone beds seen- Plectogyra between Yelkentaş and Gerence to the east of the locality known as Ker- Fusulinidae : miyan Yalısı (map section 86/1) and Eostaffella those in Şifne Peninsula and to the Parastaffella south of it (map-section 86/3) belong to There exist other limestone areas in the Lower Carboniferous (Upper Visean our district that we might include into to Lower Namurian). We are likely to the Carboniferous, besides, and in addi- place white crystalline limestones under- tion to, the Lower Carboniferous ones lying the Devonian, north of the Kara as determined through fossils listed Island, among the Lower Carboniferous above. However, we could not do so formations. because a) No fossils were found and The following fossils (determined h) lithologic data alone is not sufficient by V. Ginkel) came from compact, crys- for exact age determination. Upper parts talline limestones found in the east of of the Carboniferous are not represented Kermiyan Yalısı (map-section 86/1) : in the Peninsula. And limestones for- merly known to belong to the Paleozoic Plectogyra are now marked down as Mesozoic. Eostaffella Climacammina B. Mesozoic Paramillerella (Eostaffella) Mesozoic rocks mainly occur in lime- Endothyra stone facies. The subject matter in this Bryozoa district is the comprehensive series possibly Corals beginning with the Upper Triassic and All of the fossils named above are continuing up into the Upper Creta- found in the white, compact semi-crys- ceous (Coniacian). It covers wide areas talline limestones of the Şifne Peninsula in the map-sections 86/1 and 86/3, and as well. The brown limestone beds over- stretches in the N-S direction forming lying the white, compact limestones con- a range of mountains marked with high tained Geinitzina (Lunucammina) of the hills. It contains fossils, has gone through Paleozoic fossils, but a more exact de- various phases of the Alpine orogeny termination could not be made as to its and is cut up by a multitude of tecto- period by C. Öztemür who did the nic lines, so that any distinction of le- examination. vels does not seem possible. The following Lower Carboniferous Mesozoic (Akdağ series). — fossils (determined by V. Ginkel) were As no fossils were encountered in com- found in the brown limestones stretching pact, crystalline limestones which covered from Gerence to Yelkentaş which show the Akdağ mountains in the north no sign of crystallization and which are of the district and displayed distinct hard to tell from the Mesozoic lime- layering at places,, it has not been easy stones : to tell sections belonging to Jurassic A GEOLOGICAL STUDY IN THE KARABURUN PENINSULA 45 from those belonging to Cretaceous. So, To the southeast of Gerence, lime- for the time being, we mark these Ak- stones with dark - grey, hard crystalline dağ formations only as Mesozoic, of calcite veins, conformably underlying which there is no doubt. fossiliferous limestone beds, are found to contain : Triassic. — It is thought that the lowermost layers of the Mesozoic lime- Textularia stones in the Karaburun Peninsula be- Nodosaria long to the Upper Triassic. Trocholina Oligostegina multispira, possibly of Upper Triassic, Radiolaria and some algae, again of Triassic age, Ostracoda are found in our district. and placed in the Jurassic, which goes Dolomitic limestones (Triassic) seen to show the existence of Jurassic lime- in the Island of Sakız and the Bodrum stones stretching from Gerence to Nar- Peninsula, also occur in this district, lıca in a N-S direction. but the lack of fossils forbids calling Cretaceous. — Compact Cretaceous them Triassic for certain. Accordingly, limestones, white, grey, brown and pink we can not plot them on the map as in color, conformably overlie Jurassic Triassic formations and, what is more, limestones indicating that the c ompre- limestones near Çeşme formerly marked hensive series which probably begins in down as Triassic, now are known to the Upper Triassic continues to the belong to the Jurassic. end of the Turonian. This latter, in Jurassic. — Fossiliferous limestones turn, is overlain by the Maestrichtian of the Jurassic are widespread in our limestones beginning with a basal con- glomerate. district. The fossils listed below, and determined by C. Öztemür, come from Lower Cretaceous. — It is white crystalline limestones, pink lime- hard to distinguish the Jurassic formations stones and dolomitic limestones occurring from the white, brown, compact (also SW of Çeşme (strike N 40° E, dip 4l° stratified) Lower Cretaceous limestones SE). they conformably overlie. These Lower Coskinolinopsis a.ff.primaveus Henson Cretaceous beds dipping east cover wide Orbitopsella sp. areas in the district and are often fos- Spirocyclina sp. siliferous. They are conformably over- Textularia lain by the Cenonian deposits. The lime- Miliolidae stones, grey outside and light - grey inside, occasionally creamy, striking Mrs. Utarit Bilgütay detected Pseudo- N 30°W and dipping 54° SW form vermiporella in the white compart lime- high, pointed hills west of Çatalkaya stones and also in the brown strati- (map-section 86/1) and contain the fol- fied limestones that occur in the Köste lowing fossils, determined by V. Ginkel: Peninsula, north of Çeşme. Verneuilinidae : (cf. Dukhanio) In a formation of dark-grey lime- Miliolidae : stones striking N 20° E and dipping 44° Orbitolinidae : NW, east of Boş Island, C. Öztemür Lituolidae or Orbitolinidae : Hauarani? determined the following fossils : (Coskinolinoides) Pseudocyclarnmina Lituolidae : Haplophragmium Lituola Lagenidae : Robulus or Lenticulina Dasycladacea Ammodiscidae :Glomospira, Turritellella 46 Adnan KALAFATÇIOĞLU

Same fossils are encountered bet- the brown and white limestones lying east ween the Jurassic and Upper Cretaceous of the village of Tatarçeşme; the beige- sediments in several places within the colored limestones at the village of Yağ- district, making it possible to outline cılar north of Zeytineli village; the grey the area (if only probably) occupied, oolitic limestones at the village of Ko- by the Lower Cretaceous deposits. vanlık and the grey, finely brecciated, Upper Cretaceous.—Upper- limestones west of Oynatan. Cretaceous begins with the Cenomanian Maestrichtian- — Pink-colored sand- and conformably overlies the Lower stones and limestones overlie a basal Cretaceous. Cenomanian-Turonian lime- conglomerate of the same color, north stones, containing Trocholina cf. lenticu- of the Balıklıova village (map-section laris, are widespread in the district. The 86/1). The fossils (determined by V. Maestrichtian comes above these, on a Ginkel) that came from these deposits basal conglomerate. were : Cenomanian-Turonian.— Cenoma- Globotruncana cf. linnei nian - Turonian conformably overlies Globigerinella Lower Cretaceous and appears in lime- Verneulinidae stone facies. From a wide area, separated Buliminidae from the andesites by a fault line run- ning N-S in the east of the map - sec- Overlying these pink limestones tion 86/3, several rock samples showed with Globotruncana, are white and brown Trocholina cf. lenticularis, indicative of beds and, still further up, marly-limy Turonian age. schists. Maestrichtian flysch covers these series to the east of our district. Within The fossils below (determined by the district proper the flysch is not suf- V. Ginkel) occurred in brown, grey and ficiently pronounced to be mapped white calcite veins lying south of the separately. Either no appreciable amount Urla mineral water springs : of it was deposited, in the first place, Verneuilinidae or the greater portion is already eroded Cornuspiridae : Trocholina (Aulotortus) out. cf. lenticularis Ellipsoidinidae C. Neogene Further to the north, the following Neogene begins with a pink-colored fossils of the Lower Cretaceous were conglomerate overlying older rocks and found in black limestone beds dipping continues upward with limestone, clay, NE : marl, sand and sandstone layers inter- calated with tuff horizons. They usually Verneuilinidae strike NW-SE in the map-section 86/1 Lagenidae and dip 5° to 10° NE. Their strike is not Pithonella cf. ovalis definable in the map-section 86/3 because Glomospiridae : Glomospira of various fault lines cutting through Trocholina cf. lenticularis was re- that region. Besides the tuff beds inter- ported from a number of deposits and calated in the Neogene sediments, sili- the corresponding areas were marked ceous layers and concretions are also down as Cenomanian-Turonian. These observed. That these concretions must deposits are the well-stratified grey lime- have to do with Neogene time volcanism stones near the village of Nohutalan; is beyond doubt. A GEOLOGICAL STUDY IN THE KARABURUN PENINSULA 47

The fossils below were picked up in augite. Phenocrysts : olivine (altered, the vicinity of the town Karaburun by serpentinized, calcitized) and minerals M. Akartuna and the corresponding area opaque under the microscope (as deter- was mapped as Dacian. A number of mined by K. Markus). Lath - shaped them found also by us, could not be plagioclase cemented with augite makes determined close enough for a definite the bulk of the compact basalt deposits age setting. So the area was simply near the village of Yayla. Individual, marked down as Neogene. small size, ore veins or dikes cut through Bulimus cf. tentaculatus L. the main body. Basalt dikes near Kale- Melanopsis (Canthidomus) sp. (aff. ? cik show mercury ore mineralization. hybostoma Neum.) Basalt intrusions took place along the Melania (Melanoides) tuberculata contact zones such as limestone-schist Mull. or limestone-graywacke, etc. Lymnea (Stagnicola) sp. aff. palustris Tuffs generally occupy a large stretch corvus Gmel. of area in map-section 86/3 between Ilı- Planorbirius thiollierei Mich. ca in the west and Alaçatı part in the Alluviums south, alternating in some places with Neogene sediments. In map-section 86/1 Within our district, areas covered they lie between Kumburnu and Mor- by alluviums consist of the flat stretches doğan. near the sea shore. Balıklıova İskelesi, Çiftlik village, vicinity of Ilıca are among Serpentine. — We can not defi- them. nitely tell the age of the serpentines in the V. VOLCANISM district. Serpentine veins are seen to cut through Cretaceous formations and are Volcanic rocks are common through- found associated with radiolarite. They out the district and include mainly an- occur dark - green to black and frac- desites, basalts and tuffs, Andesites be- tured. We assume that the magmatic gin at the coastal region, along the east- activities responsible for the creation of ern side of the map-section 86/1, reach these serpentines took place during the out to cover high hills, such as Velidağ Cretaceous folding or the period im- and Kocadağ. In map-section 86/3 they mediately following it. It is most likely again cover wide areas and high spots that they belong to the Upper Cre- such as Ermeğan Mountain. They occur in taceous. all colors but generally dark. Most com- mon varieties are hypersthene, horn- VI. TECTONICS AND PALEOGEOGRAPHY blende and biotite andesites. These rocks show stratification in several places. The oldest rocks belonging to the with strikes in the direction of NNE. Devonian period, which were exposed A typical example of flow layering, run- to the Hersinian and Alpine orogenies, ning NNE, is visible on the high andesite include various argillaceous schists, ar- hills to the north of Kılıç creek. Basalts, koses, graywackes, sandstones, conglo- in the map-section 86/1 occur over the merates, quartzites and limestones. Con- wide stretch between the villages of Kü- glomerates laid down in schists, must çükbahçe and Yayla. Küçükbahçe vil- be deposited during the time when seas lage and vicinity is covered with basalts- Became shallow. Same may be assumed containing olivine. Ground mass (a light in the case of arkoses. Limestones and flow structure) : plagioclase, glass and argillaceous schists indicate periodic 48 Adnan KALAFATÇIOĞLU deepening of the Devonian sea. The ver- end of Turonian epoch this area must tical fluctuation of the sea bottom must have been covered by the sea which have been the cause of alternate layer- subsequently receded to let the land ing noticed in these deposits. All the emerge from the water in the course of Devonian strata show perfect conform-- the sub-Hersinian orogenic phase. A new ity among them, with gradual change, transgression covered the region during while passing from one into another. the Maestrichtian. Upper layers of the Lack of conformity was never observed Maestrichtian sediments were exposed in these Devonian sediments. to strong folding which gave birth to a number of small-size synclines and Differences of elasticity in differ- anticlines. This implies that the Alpine ent layers is the reason behind their orogeny had taken place during the somewhat dissimilar response to folding Late Cretaceous or a little later, while action. Devonian formations strike NNE the rocks were still sufficiently soft and and dip 30° to 60°. The Lower Carboni- the Maestrichtian limestones could un- ferous limestones overlying the Devonian dergo such strong folding. strata bear witness both to stability and depth of the seas at the time of depo- Forces acting during the Mesozoic sition. All of these series are uncon- folding in the Karaburun Peninsula formably overlain by the Mesozoic and were not unidirectional. Instead, they the Mesozoic sea lasted till the end of were localized and in most any direc- the Turonian epoch, when it finally tion. Some of folds showed NE and receded. The sea invaded the area once NW directions. again during the Maestrichtian to drain Neogene begins on older rocks with out by the close of Late Cretaceous. a red conglomerate overlain by marl, Conformable Lower Carboniferous and limestone, sandstone, clay and siliceous Devonian strata were folded during the layers with intercalations of tuff. Al- Hersinian orogeny, with folds running though the Neogene formations should NNE. have a general northwesterly trend, be- Alpine movements. — Mesozoic and cause of all the tectonic movements dur- Neogene formations showing effects of ing this period, coupled with physical the Alpine orogeny exist in the district. characteristics of these rocks, namely These sedimentary series were folded their susceptibility to folding, no such from time to time and came up from trend in any one given direction could under the sea during the sub-Hersinian, subsequently be observed. While the Laramian and Rhodanian orogenic contrary prevailed, dipping changed phases. from 10°-25°. Local tectonics of the district may Neogene tuffs and limestones occur be summarized as follows : Old Paleo- on both sides of the existing bays in zoic formations which the Hersinian the Karaburun Peninsula. These bays folding brought out of the sea sank may be said to have taken shape during down again during the Late Triassic the Neogene or later. (possibly Jurassic). M. Akartuna who worked in the At a locality called Örendere, in eastern part of our district stated that the northeast of the map-section 86/1, the Pliocene and Miocene were uncon- basal conglomerate of the Mesozoic may formably superposed showing effects of be seen overlying the Paleozoic. Till the the Alpine orogeny, effects more speci-

A GEOLOGICAL STUDY IN THE KARABURUN PENINSULA 49 fically pertaining to the Rhodanian zoic formations. Limestones form a phase. high hanging-wall on the andesite-lime- Faults. — In map-section 86/1, a stone contact, east of Tatarçeşme, lying couple of fault lines lie E-W in the N-S in the map-section 86/3. Several Mesozoic formations, south of Keplen of the faults were formed in the Neo- Mountain. Another fault line, 2 km long, gene. Fault and shore lines coincide at reaches south of Karaburun town, show- Ilıca and in the Şifne Bay. ing a hanging-wall, again in the Meso- Manuscript received February 21, 1961

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