sedimentological- stratigraphical evaluation of …

INTRODUCTION

Because of its rich coal, natural gas and qu-artz sand resources, the Thrace Basin has beenstudied in detail by various oil companies, MTAand University researchers for long years. TheTertiary units of Thrace are in general comprisedof clastics and include carbonates in shelf areas(Figure 1). TPAO conducts detailed surface andsubsurface (seismics, well log and test-develop-ment wells) studies because of the natural gasexplored in the region. Among the researchesconducted in the area, mainly Kopp et al., (1969)and Turgut et al., (1983, 1991) can be cited. Themost significant documents for the stratigraphicdefiniton of the Thrace basin are the 1:100 000scale geological maps published by the MTA(İmik, 1998; Çağlayan and Yurtseveri 1998;Şentürk and Karaköse, 1998). The Tertiary se-quence which begins to cropping out at the so-uthern foothills of the Strandja Mountains andcovers almost the whole Thrace basin, reachesup to a thickness of 900 m (Kopp et al., 1969;Turgut et al., 1983, 1991; Görür and Okay, 1996;Turgut and Eseller, 2000; Siyako, 2006). TheEocene-Oligocene units are covered by Mioce-ne and younger units in the Central and Nort-hern Thrace. İslamoğlu et al., (2008) revealedthe Oligocene paleogeography of the northernpart of the Thrace basin.

Detailed description and various age data ofthe Soğucak and Ceylan formations of the Thra-ce Basin was studied by Siyako (2006). Rese-arches conducted until today indicate that Soğu-cak formation is comprised of carbonates depo-sited in shelf environment. Besides, it was depo-sited in patchy reefal facies around Pınarhisarwhile the subsurface data show that it has cha-racteristic features of pelagic clayey limestone(Siyako, 2006). Although different ages were at-tributed to the formation in different researchesconducted in the basin, the generally acceptedage for the Soğucak formation is the Middle Eo-cene – Early Oligocene (Siyako, 2006).

During this research, facies characteristicsand age of the formation, based on fosil content,were studied in detail. According to the data ac-quired, the age of the carbonates of the Soğu-cak formation was revised; consequently theposition and the place of the formation in the ba-sin chronostratigraphy were reevaluated.

MATERIAL AND METHOD

Carbonates from the Soğucak formation arethe materials used in this research. The samplesfrom carbonates were collected along 15 me-asured stratigraphic sections where the Soğu-

Mineral Res. Exp. Bull., 139, 1-15, 2009

SEDIMENTOLOGICAL- STRATIGRAPHICAL EVALUATION OF TERTIARY CARBO-

NATES (SOĞUCAK FORMATION) OF THRACE BASIN (BOZCAADA - KIYIKÖY)

Baki VAROL*, Meltem BAYKAL** and Turhan AYYILDIZ*

ABSTRACT.- Soğucak formation which crops out in Thrace Basin has characteristics of reefal limestones and isone of the target levels in oil exploration studies in the basin. While this unit directly and unconformably overliesthe basement rocks in some areas, it is transitive to siliciclastic-dominated units (Koyunbaba formation) in otherareas. The Soğucak formation is comprised of carbonates of reefal-shore complex which was deposited in ashelf environment as a consequence of a transgression which lasted between Early-Middle Eocene and EarlyOligocene. The rocks of the lower limit of the age interval of the formation, the Lower Eocene, crops out in Boz-caada only and is transitive to Fıçıtepe formation. In general, the unit was deposited in SE of the basin betweenMiddle-Late Eocene, and between Late Eocene and Early Oligocene in NE of the basin. Sedimentological featu-res and age data indicate that Soğucak formation was deposited under the control of antecedent topography andit is the product of a time-transitive transgression together with coastal morphology and sea level changes.

Key words: Thrace Basin, Soğucak formation, sedimentology, stratigraphy

*Ankara Üniversitesi Mühendislik Fakültesi Jeoloji Mühendisliği Bölümü 06100, Ankara** MTA Genel Müdürlüğü Jeoloji Etüdleri Daire Başkanlığı Balgat, Ankara

2 Baki VAROL, Meltem BAYKAL and Turhan AYYILDIZ

Figure 1- Location map of the study area (modified from Okay and Tansel, 1992).

cak formation is observed typically. These areGökçeada, Bozcaada, Mecidiye, Süloğlu, Dol-han, Tekedere, Erenler, Soğucak, Poyralı, Okçu-lar, Akören-Pınarhisar, Manastırdere, north of Vi-ze, Kıyıköy1, Kıyıköy 1a, Kıyıköy 2 and Kıyıköy2a sections. Besides where no good outcropswere observed, point samples were collected.From these limestone samples collected alongthe sections and the points, 350 thin sectionswere prepared in TPAO Research Center. Pet-rographic and paleontological study of the thinsections were conducted both in PetrographyLaboratory of the Ankara University Departmentof Geological Engineering and Department ofGeological Research of MTA. Leica DMEP Pola-rising microscobe and Nikon E5400 Coolpix (5.1MG pixel) were used to study and to take pho-tographs of the thin sections, respectively.

STRATIGRAPHY

Stratigraphy of the Thrace Basin was studiedin detail during many researches until today(Keskin, 1974; Siyako, 2006; Siyako and Huvaz,2007). Previous studies, in general, indicate that

Middle Eocene-Early Miocene units unconfor-mably overlie the Paleozoic-Mesozoic basementin the northern parts of the basin (Esso Standart,1960; Holmes, 1961; Keskin, 1974; Kasar et al.,1983). The clastic sequence overlying the base-ment rocks were defined as the KoyunbabaMember in these studies, and the age attributedto this member is Middle Eocene (Siyako et al.,1989). Later on Keskin (1974) defined this mem-ber as Koyunbaba formation. Soğucak formationwhich overlies the Koyunbaba formation is ofMiddle-Late Eocene age in southern Thrace, na-mely in the Gelibolu peninsula, Bozcaada, Gök-çeada and Biga peninsula (Kasar et al., 1983;Sümengen et al., 1987; Temel and Çiftçi, 2002;Siyako et al., 1989). The age of the outcrops ofthe formation, at the foothills of the Strandja Mo-untains and in the northern Thrace, was in gene-ral determined as Late Eocene (Erenler, 1985;Batı et al., 1993). Besides, Önal (1985, 2002) dif-ferentiated the Early Eocene carbonates belowthe Karaağaç formation in the Gelibolu Peninsu-la as Başoğlu member. On contrary, in Kuleli-Ba-baeski paleo-rise area located in the northwest ofThrace, the age of this formation was determinedas Early Oligocene based on the well data (Kes-

kin, 1974; Siyako, 2006). Ceylan formation whichis observed to overlie these units is assumed tobe conformable in general on the Soğucak for-mation. However, in the south, in Bozcaada, theSoğucak and Ceylan formations (Kesgin and Va-rol, 2003) and in the north, around Karaburun,Soğucak and Karaburun formations (Early Oligo-cene) were observed to have unconformable re-lations (Sakınç, 1994). On these rocks, Late Eo-cene-Early Miocene Mezardere, Osmancık, Da-nişmen (Taşlısekban, Pınarhisar and Armutburnumembers) and Çantaköy formations of Yenimu-hacir Group take place. These units also are co-vered by Pliocene unconformably.

Soğucak formation which is the subject ofthis research is quite widespread in the northernparts of the Thrace Basin, and in general, theage of the unit is accepted as Middle-Late Eoce-ne as cited above. Besides, the upper section ofthe Soğucak formation in the north of the basin(around Dolhan village) was dated as Oligocene(Sirel and Gündüz, 1976).

In this study, based on descriptions madealong the measured stratigraphic sections whichare given below in detail, the age of the Soğucakformation is determined to be as Early (?)-LateEocene – Early Oligocene.

MEASURED STRATIGRAPHIC SECTIONS

The limestones of the Soğucak formationcrop out as blocks (their size varying between afew m and a 100 m) along approximately east-west lying lines in the north of the basin. Themeasured stratigraphic sections (MSS) are loca-ted in the north of the basin, beginning in thewest from Süloğlu village to Dolhan, Tekederesi,Kaynarca, Pınarhisar, Erenler, Soğucak, Vize,Okçular and around Kıyıköy in the easternmost.In the south, stratigraphic sections were measu-red on the outcrops in Bozcaada, Gökçeada;Tayfur and Mecidiyeköy. The rock samples andfossils collected along these sections were usedto evaluate the age data of the formation (Figu-res 2, 3, 4 and 5).

TERTIARY CARBONATES OF THRACE BASIN 3

Figure 2- Correlation of the formations of the measured stratigraphic sec-tions in south of the Thrace Basin.

4 Baki VAROL, Meltem BAYKAL and Turhan AYYILDIZ*

Figure 3- Chroronostratigraphic correlation of the measured stratigraphic sections insouth of the Thrace Basin.

Southern Sector of the Thrace Basin(Boz-caada, Gökçeada, Mecidiye, Tayfur)

The previous studies in the Bozcaada pointout that Soğucak formation unconformably over-lies the terrestrial Fıçıtepe formation and the ageof the of the formation is Middle Eocene (Temeland Çiftçi, 2002; Kesgin and Varol, 2003). Duringthis study, in pebblestone units of the FıçıtepeFormation small scale individual reef develop-ments were observed; this levels were observedto transite to Soğucak formation by sandstones,algae spreads and limestones with ostrea (Figu-re 6). Paleontological data acquired from thistransitive levels indicate Early Eocene (Varol etal., 2007). However, the relation of these twounits are reported to be unconformable in Meci-

diye and Tayfur regions (Siyako, 2006). Besides, Önal (1985) differentiated the levels as BaşoğluMember which could assumed to be equivalentsof the Early Eocene limestones. In this situation,it was found necessary to study the this unitwhich crops out in the Bozcaada in detail.

In Gökçeada-Kolbaşı hill the Soğucak forma-tion is represented by typical patchy reefs andthe surrounding reefs. As seen in paleontologi-cal evaluations in table 1, Late Eocene-Earlyoligocene age is attributed and its upper contactis transitive to the Ceylan formation (Figure 2).

Another section was measured around Meci-diye in the south of the basin. Here, Soğucakformation begins with algae oncoid bearingbanks and passes into coral reefs upwards. The


Figure 4a-Formations correlation of the measured stratigraphic sec-tions within the northern part of the Thrace Basin

Figure 4b-Correlation graphic of the meassured stratigraphic sectionsbelonging to the Soğucak formation within the northern partof the Thrace Basin

Baki VAROL, Meltem BAYKAL and Turhan AYYILDIZ*6

facies surroundings of the reef is represented bybioclastic limestones. Here, Soğucak limestoneunconformably overlies the basement rocks inthe Fıçıtepe formation in some places (Siyakoand Huvaz, 2007).

The last section representing the Gelibolu Pe-ninsula was measured in the north of the Tayfurvillage. The approximately 10-15 m thick limesto-nes are comprised of lenticular Nummulitesbanks and the age of the unit is Late Middle-lateEocene (Figure 3). At the basement, it has un-conformable relation with the Fıçıtepe formation.

Northern Sectodr of the Thrace Basin(between Süloğlu – Kıyıköy)

During the study conducted in Thrace Basin,the places where the Soğucak formation is di-rectly time-transgressive onto the basement areSüloğlu, Dolhan, Vize and Okçular sections. Oncontrary, in Tekedere, Manastırdere, Erenler,Soğucak and Poyralı sections it is transitive toKoyunbaba formation at the basement. The agedetermined in these sections is Late Eocene-Early Oligocene (Table 1) (Figure 5).

Along the Süloğlu section, Soğucak formati-on is unconformable on the matamorphic base-ment, along some other sections it is transitiveto a very thin (3-4 m, comprised of quartz sand-stones) Koyunbaba formation. The lower levelsare transitive to Nummulites banks from back-reef environment; at the top this carbonate as-semblage passes to coastal sandstones with10-20 m thin mudstone bands. This unit was de-fined and mapped as Taşlısekban member inprevious studies (Siyako and Kasar, 1985). La-ter on, the sequence ends up with a few metresthick Congeria-bearing limestone levels (Figure7). These limestones crop out at some distinctregions of the Thrace Basin (Kaynarca – Eren-ler) and are differentiated as Pınarhisar formati-on (Keskin, 1966; Umut et al., 1983; Umut et al.,1984). Along Dolhan section carbonates of theSoğucak formation directly and unconformablyrest on the basement. The lower levels of the se-quence begin with bank type limestones bearing

abundant Nummulites and continues with muds-tone dominated, cross bedded sandstone whichdeposited in lagoon-beach environment. It endsup with gastropoda bearing limestones whichrepresent brackish water at the top. The samp-les collected here which include abundant Num-mulites yield Late Eocene-Early Oligocene agewhich harmonize with the dating in Sirel andGündüz (1976) (Figure 4, 5).

The Tekederesi section begins with the clas-tics which unconformably rest on the basement.The sandy limestones of the Soğucak formationwith abundant bioturbation and ostrea are transi-tive to the clastic levels of the Koyunbaba forma-tion (Figure 8). The levels, in general representthe lagoonal enviroment, are followed by Num-mulites banks. In this period, based on the fastsea level changes, back-bank and fore-bank fa-cies were developed very well. This bank-typedeposition passes upwards into patchy reefswhere the coral assemblages are dominant. Inthis section, the age of the Nummulites bankswhich form the lower-middle parts was given asMiddle Eocene in previous studies (Baykal et al.,2007), however, according to latest paleontologi-cal data, age of this reefal assemblage is revisedas Late Eocene-Early Oligocene (Figure 4). Thisindicates a relative sea level increase in this areaby the end of the Eocene and beginning of EarlyOligocene (Figures 4, 5).

Along the Manastırdere section, Soğucakformation rests on the Koyunbaba formationtransitively. The first levels of the section is com-prised of reef-backreef (lagoon) assemblages.The reef assemblage that developed in later sta-ges around Kaynarca village form the massivereefal core of 50-60 m thick where the corals aredominant. In the SW direction thin bedded fore-reef facies with pelagic intercalations take place.This reefal assemblage ends up with limestonesbearing Congeria near the junction of Kaynarca-Manastır road (Figure 9).

The section measured in Soğucak villagewhich is reported as the typical section of theSoğucak formation in the Thrace Basin (Holmes,1961) massive limestone deposition developed


Figure 5a-Chronostratigraphic correlation graphic of the measured stratigraphic sectionswithin the northern part of the Thrace Basin

Figure 5b-Chronostratigraphic correlation graphic of the measured stratigraphic sec-tions belonging to the Soğucak formation within the northern part of theThrace Basin


Table 1- The age intervals of the Soğucak formation determined in measured stratigraphic sections in

the investigated region.

BOZCAADA EARLY EOCENEBryozoa, Alveolina sp. Nummulites sp.Milliolidae, Cuvvilerina sp., Discocyclina sp.,Assilina sp., Opertorbitolites douvivillei,Alveolina aff.cemali (n.s.p).

GÖKÇEADA MOST EOCENE - OLIGOCENE

Spharegypsina, Gypsina, Famiania cassis/Gyroidinella sp. Rotalidae., Asterocyclinasp., Discocyclina sp. Globigerapsis sp.Alveolina sp., Asterigerina sp., Nummulitesperfatus, Nummulites ptukhiani., Nummulitescf incrassatus, Assilina sp.,

MECİDİYE LATE EOCENEFabiania, Spiroclypeus sp., Discocyclina sp.,Nummulites sp., Gyroidinella magna

TAYFUR LATE MIDDLE - LATA EOCENEGyroidinella maga.,Fabiania cassis,Heterosteginasp., Halksyardia minima., Discocyclina sp.,Nummulites sp., Alveolina sp., Orbitolites sp. ,Acervulina sp.,

SÜLOĞLU LATE EOCENE - EARLY OLIGOCENECongeria sp., Gastropoda, Coral, Red algBryozoa, Nummulites sp.,

DOLHAN LATE EOCENE - EARLY OLIGOCENENummulites intermedius, Nummulites ficteli,Nummulites vascus, Asterigerina sp., Operculinasp., Rotalia sp., Nummulites fabianii., Fabianiacassis.,

TEKEDERE LATE EOCENE - EARLY OLIGOCENEFabiania cassis, Gyroidinella cf-magna.,Acervulina. sp, Miliolidae., Spiroclypeus sp.,Nummulites cf., vascus Planispira sp.,Textularia sp., Bryozoa, K›rm›z› alg

MANASTIRDERE LATE EOCENE - EARLY OLIGOCENERed algea, Nummulites sp., Miliolidae,Pelecypoda Asterigarina cf rotulaTextularidae, Nummulites vascus Rotalia cfarmata Ostrokoda, Pelecypoda

ERENLER LATE EOCENE - EARLY OLIGOCENENummulites sp., Nummulites cf. yascusNummulites cf., fichteli, Red algea, BryozoaNummulites sp.

SOĞUCAK LATE EOCENE - EARLY OLIGOCENERed algea, Ekinit, Nummulites sp.,Miliolidae, Pelecypoda, MercanAmhisteginid, Rotalidae., Sphaerogypsinasp., Nummulites cf. vascus, Nummulites sp.,

VİZE LATE MOST EOCENE - EARLY OLIGOCENEGyroidinella magna, Acervulina., Miliolidae,Orbitolites sp, Asterigerina sp., Rotalia sp.,Nummulites cf., vascus Gyroidinella sp.,Asterigerina rotula, SpiroclypeusChapmanina gassinensis, Alveolinidae,Fabiania sp.,

OKÇULAR LATE EOCENENummulites cf, fabiani, Asterigerina sp.Discocyelina sp. Orbitolites sp.,Heterostegina sp., Rotalidae, Miiolidae,Ostracoda, Nummulites sp.,

BALKAYA LATE EOCENERed algea, Nummulites sp., Amphisteginid,Miliolidae,

KIYIKÖY 1 LATE EOCENE - EARLY OLIGOCENERed algea, Nummulites sp., Coral., Bryzoa,Pelecypoda, Nummulites cf. VascusCytheridae cf. pernota, Costa tricostataPaijenborchella sp.,

KIYIKÖY 2 OLIGOCENENummulites sp., vascus Operculina? sp.Operculia cf. Complanata Amphisteginid,Krithe cf., bartonensis, Cytheretta tenuistriataCosta tricostata, Ruggieria sp., Cytheridae

KIYIKÖY 3 OLIGOCENENeorotalia lithothamnica, Nummulitesfichteli, Nummulites vascus,Nummulites sp.,Ekinit, Pelecypoda., Red algea

KIYIKÖY 4 LATE EOCENE - EARLY OLIGOCENENeorotalia lithothamnica, Nummulites cf. vas-cus Oeprculina? sp. Operculia cf. complanata,Amphisteginid Krithe cf. bartonensis,Cytheretta tenuistriata, Cytheridae Cytherettatenuipunctata, Costa tricostata, Ruggieria sp.

MEASURED SECTIONLOCATION

AGE INTERVAL IN THISSTUDYFOSSIL CONTENT

9TERTIARY CARBONATES OF THRACE BASIN

Figure 6- Transition of Fıçıtepe – Soğucak formations in south of Bozcaada – Poyrazport.

Figure 7- Transition of Soğucak formation – Taşlısekban Member in (northof) Süloğlu.


Figure 9- Transition from reefal Soğucak limestone to Congeria bearing limestone in the Manastır section(north of the Kaynarca village).

in form of bank-reef complex is observed. Aro-und this assemblage, back-reef and fore-reef fa-cies spread out in wide areas. In this area, on-laps and offlap sets which indicate fast sea levelchanges overlie each other angularly. Datingfrom the samples collected from the entire sequ-ence indicate Late Eocene-Early Oligocene(Table 1). Along the Erenler section which is lo-cated at the southeastern extension of this sec-tion, this reefal assemblage is covered by 5-7 mthick cross bedded ooliitic limestones. Thetransgressive layering observed in oolites whichrepresent the carbonate shoal indicate the chan-ges in the coast line based on the sea level chan-ges. The Congeria sp. bearing limestones whichform the uppermost level of the section representa brackish water facies that developed in theplatform where the Soğucak formation was de-

posited; its stratigraphical position is interpretedas the upper section of the formation.

Paleontological determinations indicate thatage of the unit is Late Eocene-Early Oligocene(Figure 5, Table 1).

In the north of Vize, the Soğucak formationunconformably overlies the basement rocks. Inthis section which displays examples of a a typi-cal bank formation, the E-W trending massivebank and the surrounding facies represented bythin to medium limestones are observed (Figure8). The back-bank facies deposited during theregressional periods are in general thin beddedand include carbonaceous mudstone intercalati-ons and abundant bioturbations (Figure 10). Theage interval of the formation, different from theprevious studies (Baykal et al., 2007: Middle Eo-

Figure 8- The facies and stratigraphic relation of the Soğucak formation with the other units in the Tekederesisection.

cene) but conformable with the other sections,was determined as Late Eocene – Early Oligo-cene (Figures 4, 5) (Table 1).

The Soğucak formation which can be obser-ved in the easternmost part of the study areacrops out around the Kıyıköy and was investiga-ted by sections measured on both flanks of an an-ticline observed on the coast. The sequence un-conformably rests on the basement rocks andthere is a thin siliciclastic-dominant level at thebase of the formation. In the overlying coastsandstones (5-10 m thick) with bioturbation,mudstones including mud intraclasts and flamestructures representing tide conditions take place.This level passes upwards into cross beddedclastic limestones (Figure 4). This clastic sectionis 10-15 m thick and includes a few meter thick in-dividual coral reefs. The sequence ends up withlevels bearing Ostrea and gastropoda depositedalong a retreading coast line. This way, the levelsincluding mudstone intercalations pass into theCeylan formation through a tuffaceous level (Fi-gure 11).

Section (2, 2a) represents the southern flankof the syncline. Sandy limestone with bioturbati-on is located at the base similarly (10 - 15 m).This level passes upwards massive bioclasticsand and sandstone with coral fragments. Atthese levels many soft deformation structuresand brecciation and nodules are observed. Inthis section which is about 50 m thick channelsfills with pebbles, cross bedding and local inter-bands with echinoid lineaments can be obser-ved. The sequence in general is of set sandcomplex nature. In the back-set abundant pe-lecypod, Ostrea and gastropoda bearing biotur-bated sandy limestone and carbonate mudsto-nes were deposited. The most typical examplesof bioclastic dominated Soğucak formation is re-vealed in this section. Along the coast, NW-SEtrending limestones with huge cross beds mostprobably mark the megaripples active along thecoast line (Figure 4).

The age interval which is valid fort he wholeKıyıköy section is determined as Late Eocene(Priabonian) –Oligocene (Rupelian – Early Chat-tian) (Baykal et al., 2009) (Table 1) (Figure 5).


Figure 10-Facies assamblages of the Soğucak formation in the north of the Vize


Figure 11- Facies assemblages representing the transition of the Soğucak – Ceylan for-mations in the Kıyıköy.

COMPARISON OF THE MEASURED

STRATIGRAPHIC SECTIONS

Southern Sector: In this sector, the Bozcaa-da, Gökçeada, Tayfur (in Gelibolu Beninsula)sections and Mecidiye section (Gulf of Saros)were measured. The most different section hereis the Bozcaada section; abundant Alveolina ca-navari, Alveolina pasticillate, Alveolina aff. pisi-formis, Alveolina avellena, Alveolina cemali, Al-veolina sp., and Nummulites sp., (Table1) fossilsare dominant throughout the bank-type limesto-nes in the unit which was determined to beMiddle Eocene Soğucak formation previously.However the above mentioned fossils indicateEarly Eocene (Figure 3). Another different pointis about the lower boundary of the Soğucak for-mation. In previous studies, Fıçıtepe formationis defined as aterrestrial formation in the region.In this study, it was observed that the upper bo-undary of the formation is composed of beach

pebblestones-micro reefal assemblage, and it istransitive with the Soğucak formation (Varol etal., 2007). Although in the Gökçeada, Mecidiyeand Tayfur sections Fıçıtepe formation is uncon-formably located at the lower boundary of theSoğucak formation, especially in the Mecidiyesection, it can directly overlie the basementrocks as a result of time transgression. Age ofthe unit defined in these sections is Middle-LateEocene. In all the sections, Ceylan formationconformably take place at the upper boundariesof these sections (Table 1) (Figures 2-3).

Northern Sector: When a west to east orde-ring was made here, the first group is represen-ted by the Süloğlu, Dolhan and Tekedere secti-ons. The age interval determined as Late Eoce-ne – Early Oligocene (Figure 5). In these secti-ons the Early Oligocene (?) Soğucak formation(Late Eocene in Dolhan stream) unconformablyoverlies the basement. However, along the other


sections, clastics of the Koyunbaba formationare transitively located at the base. The uppercontact of the formation is variabe in this region.In the Süloğlu, in a limited area, quartz sandsto-ne and mudstone which are the products of a si-liciclastic coastal development overlie the plat-form limestone (Taşlısekban formation) and thisis overlain by Congeria bearing limestones (Pı-narhisar formation). Extensions of these two for-mations which overlie the Soğucak formation arenot observed in this position along the other sec-tions. Only in the Dolhan stream a formation si-milar to the Pınarhisar is observed to overlie theSoğucak formation (Table 1). In the Tekederestream this upper section is missing (Figure 4).

Northeastward, along the Manastırdere, Ça-yırdere, Erenler and Soğucak sections the Ko-yunbaba formation is observed at the base.Along Okçular section, Soğucak formation is ob-served to overlap the basement. Age of the So-ğucak formation determined here is in generalLate Eocene – Early Oligocene, however, alongthe Okçular section it is Late Eocene. Erenlersection has a difference in this group (Figure 4).The oolitic facies and the Congeria bearing li-mestone in the section are not observed alongthe other sections. In previous studies these fa-cies assemblage is mapped as the Pınarhisar(Keskin, 1966).

Along the Vize and Kıyıköy sections whichare located at the easternmost part of the studyarea Soğucak formation is unconformable onthe basement, however, along the section Kıyı-köy 1a, a thin (3-5 m) siliciclastic level behindthe Soğucak formation can be correlated to theKoyunbaba formation with its stratigraphic posi-tion. The age interval obtained from these secti-ons is Late Eocene – Early Oligocene (Table 1,Figure 5). A significant matter that should bementioned here is that Kıyıköy facies is quite dif-ferent than the other facies assemblages in theareas of the other section with respect to the fa-cies types and environments (shore, back-sho-re, beach, lagoon). The upper limit of the Soğu-cak formation passes by a thin tuffaceous level

in lagoon facies to the Ceylan formation in Kıyı-köy (Figure 11).

DISCUSSIONS AND RESULTS

Soğucak formation which crops out in theThrace was deposited as reefal facies in gene-ral between Middle Eocene – Early Oligocene.The Nummulites banks, from the point of faciesdevelopment, dominantly characterizes theMiddle – Late Eocene. The dominant coralpatchy reefs were deposited during Late Eocene– Early Oligocene. The facies around reefs haveformed different deposition environments basedon the sea level changes. These can be differen-tiated as back-reef – lagoon, tidal flat, oolite sho-als and fore-reefs.

Soğucak formation was deposited in EarlyEocene in the Bozcaada section. If this time in-terval is taken as a beginning point, it can be sa-id that the Eocene transgression in the Thracebasin has advanced on an irregular topographytime transgressively from south to north. For thisreason, in the Kıyıköy which is the distant pointof the transgression, a thick Oligocene sequen-ce was deposited. The depositional features andage limits of the Soğucak formation pointed outin this study emphasize the necessity to dealwith the following subjects:

1- The Early Eocene limestones cropping outin the Bozcaada were included in Soğucak forma-tion, however, this unit must be studied in detailand its position in the Eocene must be clarified.

2- Interpretation of oolite and Congeria bea-ring limestones which were assumed to be a dis-tinct facies group in the Soğucak formation inthe Kaynarca-Erenler section as a different faci-es assemblage deposited in the platform wherethe Soğucak formation was deposited, and con-sequently its redefinition as a single formation(Soğucak Fm); this redefinition shall facilitate thecorrelation of Early Oligocene units which cropout widespreadly in the Soğucak formation.


3- The units which rest on the basement inthe Kıyıköy are quite different than the facies de-fined in the Soğucak formation. In the regionwhich is represented by high energy clastic car-bonate depocenters (set island – beach comp-lex, megaripples, etc.) detailed sedimentologicalstudies are required.

ACKNOWLEDGEMENT

The authors thank TÜBİTAK for its contributi-on in realizing this study (Project no. 104Y333)and Dr. Ercüment Sirel (Ankara University) whocarried out the paleontological determinationsand Mr. Muzaffer Siyako (TPAO) for his remarkson the study.

Manuscript reacived February 2, 2009

REFERENCES

Batı, Z., Erk, S., and Akça, N., 1993. Trakya hav-zası Tersiyer birimlerinin palinomorf, fo-raminifer ve nannoplankton biyostratig-rafisi. TPAO Araştırma Merkezi Grubu, Rapor no:1947, 92 p. Ankara, (unpublis-hed).

Baykal, M., Varol, B., and Ayyıldız, T., 2007. Ku-zey Trakya Soğucak Formasyonu’ nunsedimantolojisi. 60. Türkiye Jeoloji Ku-rultayı Bildiri Özleri, 358, Ankara.

______, ______, and _____., 2009. Kıyıköy veyakın civarında (KD Trakya) SoğucakFormasyonu’ nun ortamsal değerlendi-rilmesi. 62. Türkiye Jeoloji Kurultayı Bil-diri Özleri Kitabı-I, 324-325, Ankara.

Çağlayan, M.A., and Yurtsever, A., 1998. Bur-gaz-A3, Edirne-B2 ve B3; Burgaz-A4 ve Kırklareli-B4, Kırklareli-B5 ve B6, Kırkla-reli-C6 paftaları, 1:100000 ölçekli açın-sama nitelikli Türkiye Jeoloji haritaları,No:20,21,22,23 MTA, Ankara.

Erenler,M., 1985. Trakya baseni merkezi kısmın-da seçilen kuyuların mikropaleontolojive biyostratigrafileri. TPAO Araştırma

Merkezi Grubu, Rapor no: 809. Ankara(unpublished).

Esso Standard, 1960. I sayılı Marmara petrolbölgesi AR/EST/105,106, 108 ve 109hak sıra numaralı sahalara ait terk rapo-ru. TPAO Arama Grubu, Rapor no:1031. Ankara, (unpublished).

Görür, N and Okay, A.I., 1996. Fore – arc originof the Thrace basin, northwest Turkey.Geologische Rundschau, 85, 662-668

Holmes, A.W.,1961. Stratigraphic review of theThrace. TPAO Rapor no: 368. Ankara,(unpublished).

İmik, M, 1988. Kırklareli-C2-3 Paftası ve İzahna-mesi, 1:100 000 ölçekli Türkiye JeolojiHaritaları. Maden Tetkik ve Arama Ge-nel Müdürlüğü, Ankara 10 p.

Islamoğlu, Y., Harzhauser, M., Gross, M., Ji-me´nez-Moreno, G., Coric, S., Kroh, A.,Rögl, F., and van der Made, J., 2008.From Tethys to Eastern Paratethys: Oli-gocene depositional environments, pa-leoecology and paleobiogeography ofthe Thrace Basin (NW Turkey).

Kopp, K.O., Pavoni,N and Schindler,C., 1969.Geologie Thrakiens IV: Das Ergene-Becken. Beih zum Geol.Jahrb.,Heft76,136 p., Hannover.

Kasar, S., Bürkan, K., Siyako, M., and Demir, O.,1983. Tekirdağ - Şarköy - Keşan - Enezbölgesinin jeolojisi ve hidrokarbon ola-nakları. TPAO Arama Grubu, Rapo rno:1771, 71 p. Ankara, (unpublished).

Keskin, C., 1966. Pınarhisar resif karmaşığı mik-rofasiyes incelemesi. Rev. Fac. Scien.Univ. İst., Seri B,31/3 -4, 109-146.

______, 1974. Kuzey Trakya havzasının stratig-rafisi. Türkiye İkinci Petrol Kongresi Tebliğleri Kitabı, 137-163.

Kesgin, Y., and Varol, B., 2003. Gökçeada veBozcaada’nın Tersiyer Jeolojisi (Çanak-kale). Maden Tetkik ve Arama Dergisi,126, 49-68.

Okay, A.I. and Tansel, İ., 1992. Pontid-İçi Okya-nusunun Üst Yaşı Hakkında Şarköy Ku-zeyinden (Trakya) Yeni Bir Bulgu. Ma-den Tetkik ve Arama Dergisi, 114, 21-24.

Önal, M., 1985. Gelibolu (Çanakkale) kuzeybatı-sının jeolojisi. Doktora Tezi, İstanbul Üni-versitesi, Jeoloji Müh. Bölümü, İstanbul,200 p.

______, 2002. Başoğlu Üyesi’nin Litostratigrafi-si (Gelibolu Yarımadası), Trakya Bölge-si’nin Litostratigrafisi adlamaları; Türki-ye stratigrafi komitesi 2. Çalıştayı, MTA,7, Ankara.

Sakınç, M., 1994. Karaburun (B İstanbul) deni-zel Oligosen'inin stratigrafisi ve paleon-tolojisi. Maden Tetkik ve Arama Dergisi,116, 9-14.

Sirel, E. and Gündüz, H., 1976. Kırklareli (KuzeyTrakya) denizel Oligosen’in stratigrafisive Nummulites türleri. TJK Bülteni,19/2, 155-158.

Siyako, M., 2006. Trakya Bölgesi Stratigrafi Ko-mitesi Litostratigrafi Birimleri Serisi-2,43-83. MTA Genel Müdürlüğü, Ankara.

______, Bürkan, K. and Okay, A., 1989. Biga veGelibolu yarımadalarının Tersiyer jeolo-jisi ve hidrokarbon olanakları. TürkiyePetrol Jeolohları Derneği Bülteni, 1,183-199.

Siyako, M. and Huvaz, O., 2007. Eocene Stra-tigraphic Evolution of the Thrace Basin, Turkey. Sedimentary Geology, 198,75–91.

Şentürk, K. and Karaköse, C., 1998. Çanakkale-D2 Paftası, 1:100 000 ölçekli açınsamanitelikli Türkiye jeoloji haritaları, No: 62.MTA Genel Müdürlüğü, Ankara.

Sümengen, M., Terlemez, İ., Şentürk, K., Kara-köse, C., Erkan, E.N., Ünay, E., Gürbüz,M., and Atalay, Z., 1987. Gelibolu yarım-

adası ve güneybatı Trakya TersiyerHavzasının stratigrafisi, sedimantolojisive tektoniği. MTA Genel Müdürlüğü Ra-por no:8218 (unpublished).

Temel, V. and Çiftçi, N.B., 2002. Gelibolu yarım-adası Gökçeada ve Bozcaada TersiyerÇökellerinin Stratigrafisi ve OrtamsalÖzellikleri. Türkiye Petrol JeologlarıDerneği Bülteni,14,17-40, Ankara.

Turgut, S., Siyako, M., and Dilki, A., 1983. Trak-ya havzasının jeolojisi ve hidrokarbon olanakları. Türkiye Jeoloji Kongresi Bül-teni, 4, 35-46.

Turgut, S.,Türkaslan, M., and Perinçek, D.,1991. Evolution of the Thrace sedimen-tary basin and its hydrocarbon prospec-tivity. In: Spencer AM (ed) Generation,accumulation, and production of Euro-pes hydrocarbons. Special Publicationof European Association of PetroleumGeoscientists,1, 415-437.

_____ and Eseller, G., 2000. Sequence stratig-raphy, tectonics and depositional historyin Eastern Thrace Basin, NW Turkey.Marine and Petroleum Geology, 17, 61 -100.

Umut, M., Kurt, Z., İmik, M., Özcan, İ., Sarıkaya,H., and Saraç, G., 1983. Tekirdağ, Siliv-ri (İstanbul), Pınarhisar alanının jeoloji-si: MTA Derleme no: 7349. Ankara, (un-published).

______, ______, ______, Ateş, M., and Saraç,G., 1984. Edirne-Kırklareli-Lüleburgaz-Uzunköprü civarının jeolojisi: MTA Der-leme No: 7604. Ankara, (unpublished).

Varol, B., Sirel, E., Ayyıldız, T., and Baykal, M.,2007. Bozcaada’da (Çanakkale) Soğu-cak Formasyonun’da saptanan yeni pa-leontolojik ve sedimantolojik Bulgular.Maden Tetkik ve Arama Dergisi, 135,83-86.

15TERTIARY CARBONATES OF THRACE BASIN

INTRODUCTION

Ereğli-Ulukışla Basin is located 100 km NWof the Adana city (Figure 1). Güney formationwhich forms part of the basin spreads out in Ulu-kışla (Niğde), Çamardı, Pozantı and Ereğli (Kon-ya) (Figure 1).

The basin is delimited by Aladağlar mounta-ins and Ecemiş fault in the east, by Niğde mas-sif in the west and by Bolkar mountains in thesouth (Demirtaşlı et al., 1973) (Figure 1).

Geological studies for different purposes we-re carried out in the study area and surroundings(Ketin and Akarsu (1965), Demirtaşlı et al.,1973;Oktay, 1982; Dellaloğlu and Aksu, 1986; Pampaland Meriç; 1990; Sonel and Sarı, 2004; Dursun,2006). This study aims to reveal the nannoplank-ton biostratigraphy of the study area in detail.

In study area and its surroundings an ophioli-tic emplacement is observed in Late Cretaceo-us; following this a sedimentary sequence weredeposited in Late Cretaceous – Miocene time in-terval. The units filling the basin are clastic de-posits, volcanosedimentary units, carbonates

and evaporites. There are vertical and horizontaltransitions and lithofacies changes among theUlukışla, Halkapınar, Hasangazi and Güney for-mations (Figure 2). These units are shown in fly-sch character and they include many channel fil-ling structures (Sonel and Sarı, 2004). By theend of the Middle Eocene, as a result of tectonicmovements, the region has gained its structuralposition as shown today.

In this study, nannoplanktons in 50 samplescollected from a measured stratigraphic sectionin Güney formation were studied and taxons of5 biozone were determined (Figure 3). Thesedata indicate that age of the formation is Selan-dian – Ypresian (Paleocene – early Eocene).

MATERIAL AND METHOD

50 samples collected from the Güney forma-tion along a measured stratigraphic section arethe materials used in this study. Slides were pre-pared from the samples by stripping method.Abundance of zone fossils from the samples col-lected were counted in 200 areas (Wei, 1988)and revealed. Accordingly, following evaluation

NANNOPLANKTON BIOSTRATIGRAPHY OF THE SELANDIAN-YPRESIAN GÜNEY

FORMATION (ULUKIŞLA BASIN) AND SEA-WATER TEMPERATURE CHANGES IN

THIS PERIOD

Manolya SINACI* and Vedia TOKER**

ABSTRACT.- In this research, nannoplankton flora of Selandian-Ypresian Güney formation which is comprisedof sandstone-shale intercalation and cropping out in Ereğli – Ulukışla basin was studied. 44 species of 16nannoplankton taxons were determined in 50 samples collected from Güney measured stratigraphic section.Flora of five nannoplancton zone [(Fasciculithus tympaniformis Zone (late Selandian), Heliolithus kleinpelliiZone (late Selandian – early Thanetian, Heliolithus ridelii Zone (Thanetian), Discoaster multiradiatus Zone(Thanetian), Tribrachiatus contortus Zone (Ypresian)] were determined. Of the nannoplancton species whichare sensitive to temperature changes, Coccolithus eopelagicus indicate mild – cool water and Discoaster andSphenolith indicate mild-warm water environments; based on this information, we suggest that the sea waterduring the Selandian was mild to warm, during the Thanetian, the sea water was mild to cool and during theYpresian, again the mild to warm sea water conditions prevailed.

Key words: Nannoplankton, Güney formation, Ereğli-Ulukışla Basin, Selandian, Ypresian.

*Ankara Üniversitesi, Mühendislik Fakültesi, Jeoloji Mühendisliği Bölümü 06100,Ankara**Adıyaman Üniversitesi


18 Manolya SINACI and Vedia TOKER

Figure 1- Location map of the study area (MTA, 2002)

was made for the species: one or many speciesin an area as “Abundant = B”; one species in 2 -10 areas as “Widespread = Y”, and one speciesin 11 – 50 areas as “ Few (Little) = A” and onefrom each species in 51 – 200 areas as “Rare =N” (Table 1).

LITHOSTRATIGRAPHY

Güney formation which crops out in studyarea is comprised of an intercalation of sandsto-ne and shale, however, red lenticular mudstonesand thin to medium bedded lenticular sandsto-nes and mudstones are also included. Pillow la-vas of 1 – 15.5 m thick are also observed in the

ULUKIŞLA BASIN NANNOPLANKTON BIOSTRATIGRAPHY 19

Figure 2- Generalized stratigraphic columnar section of the Ereğli-UlukışlaBasin(Dursun, 2006).

unit. At the top of the unit widespread lenticularchannel fills displaying graded bedding, slumpdeposits and intercalations of turbiditic sandsto-ne are observed.

Güney formation is represented very wellaround Ulukışla – Güney village. It was develo-

ped time regressive from north to south; therefo-re it has different facies and ages around its typi-cal locality and southwest of Ulukışla (Oktay,1982).

Güney formation was deposited in generalbelow the wave base and by turbiditic currents.


Figure 3- Generalized view ıof Güney formation (north of Bekçitepe).

The lower levels of the sequence include chan-nel fills and sandstones are dominant in theselevels, therefore they display characteristics ofproximal turbidites. Northward in the study area,the shale and sandstone dominance becomeequal; in these regions channel fills are obser-ved at the upper sections and sandstones beco-me dominant with coarse grains while the domi-nance of the shales decrease. For this reason,the upper levels are observed in proximal turbi-ditic character.

The unit was developed in general as grey,coarse sandstone and shale intercalation. It is800 m thick.

Güney formation is vertically and horizontallytransitive to Ulukuşla and Halkapınar formationsin the study area. It is not observed south of Ulu-kışla, but here Hasangazi formation which hasthe same age with the Ululışla formation was de-posited. Aktoprak formation is vertically and ho-rizontally transitive to Hasangazi and Güney for-mations and overlies these two formations. Mi-ocene – Pliocene Cihanbeyli formation uncon-formably overlies the Aktoprak formation in so-uth, and Güney formation in the north of thestudy area.

Along the 652 m thick Güney stratigraphicsection which is comprised of sandstone – sha-le intercalation, between 58 – 78 m the amount


Table1- Abundance of Güney formation nannoplankton zone species


of sandstone decreases while the shales increa-se. Between 78 – 111 m, the thickness of sand-stones is more than that of the shale (Figure 3).

BIOSTRATIGRAPHY

16 genus and 44 species were determinedalong 652 m thick stratigraphic section in Güneyformation, and 5 biozones were defined (Figure3). In the first 58 m, Fasciculithus tympaniformisZone ranging between the first appearance ofFasciculithus tympaniformis Hay and Mohlerand the first appearance of Heliolithus kleinpelliiSullivan; between 58-78 m Heliolithus kleinpelliiZone ranging between the first appearance ofHeliolithus kleinpellii Sullivan and Discoastergemmeus Stradner; and between 78-111 m He-liolithus rideli Zone ranging between the first ap-pearance of Heliolithus ridelii Bramlette and Sul-livan or Dicoaster nobilis Martini and Discoastermultiradiatus Bramlette and Riedel; between111-621 m Discoaster multiradiatus Zone ran-ging between the first appearance of Discoastermultiradiatus Bramlette and Riedel and Tribrac-hiatus contortus Stradner, between 621-652 mTribrachiatus contortus Zone ranging betweenthe first and last appearance of Tribrachiatuscontortus Stradner were determined (Figure 4,Table 1.2). As for the previous studies related tothe biostratigraphic zoning of nannoplanktonswe can cite Hay and Mohler (1967), Bukry(1969), Martini (1971), Okada and Bukry (1980)and, Perch and Nielsen (1985 a, b). This studyis based on the standard zoning of Perch andNielsen (1985 a, b) (Table 1,2).

Fasciculithus Tympaniformis Zone

Description: Zone was formed during the in-terval between the first appearance Fasciculit-hus tympaniformis Hay and Mohler and the firstappearance of Heliolithus kleinpellii Sullivan of(Plate I, Figure 6).

Author: Hay and Mohler (1967)

Category: Concurrent range zone

Stratigraphic level: Selandian

Fossil Assemblage: Biantolithus sparsus(Bramlette and Martini), Coccolithus eopelagi-cus (Bramlette and Riedel), Discoaster barbadi-ensis (Tan Sin Hok), Ericsonia cava (Hay andMohler), Ericsonia ovalis (Black), Ericsonia ro-busta (Bramlette and Sullivan), Fasciculithustympaniformis (Hay and Mohler), Fasciculithusinvolotus (Bramlette and Sullivan), Sphanolithusradians (Deflandre), Sphenolithus anarrhopus(Burky and Bramlette), Toweius tovae (Perchand Nielsen), Thracosphaera sp. (Kamptner)and Zygrhablithus bijugatus (Deflandre).

Comparison and Interpretations: Hay andMohler (1967), Martini (1971), Perch and Niel-sen (1972,1985a), Toker (1977), Okada andBukry (1980), Aköz (1981), Meriç et al. (1987),Lang and Wise (1987), Wise and Pospichal(1990), Aydın (2005) defined this zone at the sa-me stratigraphic level during their studies. Du-ring this study, Fasciculithus tympaniformis Zo-ne is determined in Selandian (Table 2).

Heliolithus Kleinpellii Zone

Description: Heliolithus kleinpellii Zone wasformed during the first appearance of Sullivanand Discoaster gemmeus Stradner (Plate I, Fi-gure 2).

Author: Hay and Mohler (1967)


Stratigraphic level: Upper level of late Selan-dian – lower level of early Thanetian

Fossil Assemblage: Coccolithus eopelagicus(Bramlette and Riedel), Discoaster barbadiensis(Tan Sin Hok), Ericsonia cava (Hay and Mohler),Ericsonia ovalis (Black), Ericsonia robusta(Bramlette and Sullivan), Fasciculithus tympani-formis (Hay and Mohler), Heliolithus kleinpellii(Sullivan), Sphenolithus anarrhopus (Burky andBramlette), Toweius tovae (Perch and Nielsen).

Comparison and interpretation: Hay andMohler (1967), Bukry (1969), Martini (1971),

23ULUKIŞLA BASIN NANNOPLANKTON BIOSTRATIGRAPHY

Perch and Nielsen (1972,1985a), Toker (1977),Okada and Bukry (1980), Aköz (1981), Lang andWise (1987), Wise and Pospichal (1990), Aydın(2005) defined this zone during their studies. Onthe other hand, Decima et al. (1975) definedthis zone as Markalius inversus Zone. Meriç etal. (1987) could not determine this zone duringtheir study. In this study Heliolithus kleinpellii Zo-ne was determined in late Selandian-early Tha-netian based on the findings and the study ofBukry (1969) (Table 2).

Heliolithus Ridelii Zone

Description: Heliolithus ridelii Zone was for-med between the first appearance of Heliolithusridelii Bramlette and Sullivan or Dicoaster nobilisMartini and the first appearance of Discoastermultiradiatus Bramlette and Riedel (Plate I, Fi-gure 3).

Author: Bramlette and Sullivan (1961),Perch-Nielsen (1972)


Stratigraphic level: Thanetian

Fossil Assemblage: Coccolithus eopelagicus(Bramlette and Riedel), Cribrocentum reticula-tum (Gartner and Smith) Perch and Nielsen,Discoaster aster (Bramlette and Riedel), Ericso-nia formousa (Kamptner), Ericsonia ovalis(Black), Fasciculithus tympaniformis (Hay andMohler), Heliolithus ridelii (Bramlette and Sulli-van), Sphenolithus anarrhopus (Burky andBramlette), Sphenolithus editus (Perch-Niel-sen), Sphenolithus primus (Perch and Nielsen),Sphenolithus radians (Deflandre), Toweius to-vae (Perch and Nielsen), Tribrachiatus orthost-ylus (Shamrai) and Thracosphaera sp.

Comparison and interpretation: Hay andMohler (1967), Bukry (1969), Martini (1971),Decima et al. (1975), Perch and Nielsen(1985a), Wise-Pospichal (1990), Aydın (2005)defined this zone during their studies. On the ot-her hand, this zone was defined as Discoastergemmeus Zone by Toker (1977) and Aköz

(1981). Perch and Nielsen (1972), Okada andBukry (1980), Lang and Wise (1987) defined thiszone as Discoaster nobilis Zone. Meriç et al.(1987) determined the fosil assemblage of thiszone durng their study. In this study, Heliolithusridelii Zone is determined as Thanetian basedon the findings and the study of Bukry (1969)(Table 2).

Discoaster Multiradiatus Zone

Description: Zone was formed between thefirst appearance of Discoaster multiradiatusBramlette and Riedel and first appearance of Trib-rachiatus contortus (Stradner) (Plate, Figure D).

Author: Bramlette and Sullivan (1961), Marti-ni (1971)


Stratigraphic level: Upper level of Late Tha-netian

Fossil Assemblage: Biantolithus sparsus(Bramlette and Martini), Braarudosphaera bige-lowi (Gran and Braarud), Coccolithus eopelagi-cus (Bramlette and Riedel), Chiasmolithus dani-cus (Brotzen), Chiasmolithus solithus (Bramletteand Sullivan), Cribrocentum reticulatum (Gart-ner, 1967), Cruciplacolithus tenius (Stradner)Hay and Mohler, Discoaster aster (Bramletteand Riedel), Discoaster barbadiensis (Tan SinHok), Discoaster deflandrei (Bramlette and Rie-del), Discoaster diastypus (Bramlette and Sulli-van), Discoaster elegans (Bramlette and Sulli-van), Discoaster gemmeus (Stradner), Discoas-ter multiradiatus (Bramlette and Riedel), Disco-aster pacificus (Haq), Discoaster salisburgensis(Stradner), Ericsonia cava (Hay and Mohler),Ericsonia formosa (Kamptner), Ericsonia robus-ta (Bramlette and Sullivan), Ericsonia ovalis(Black), Fasciculithus involotus (Bramlette andSullivan), Fasciculithus tympaniformis (Hay andMohler), Heliolithus kleinpelli (Sullivan), Heliolit-hus ridelii (Bramlette and Sullivan), Micrantolit-hus crenulatus (Bramlette and Sullivan), Marka-lius inversus (Deflandre), Neochiastozygus eo-seapes (Perch and Nielsen), Neochiastozygus


Table 2- General comparison of Paleocene – Early Eocene nannoplankton zones.

junctus (Bramlette and Sullivan), Pontosphaeraplana (Bramlette and Sullivan), Sphenolithusanarrhopus (Burky and Bramlette), Sphenolithusconspicuus (Martini), Sphenolithus editus(Perch and Nielsen), Sphenolithus primus(Perch and Nielsen), Sphenolithus radians (Def-landre), Toweius tovae (Perch and Nielsen),Thracosphaera sp., Toweius eminens (Bramlet-te and Sullivan), Tribrachiatus orthostylus(Shamrai) and Zygrhablithus bijugatus (Deflan-dre).

Comparison and interpretation: Hay andMohler (1967), Bukry (1969), Martini (1971),Perch and Nielsen (1972,1985a), Decima et al.(1975), Toker (1977), Okada and Bukry (1980),Aköz (1981), Meriç et al. (1987), Lang and Wise(1987), Wise and Pospichal (1990), Aydın(2005) defined this zone at the same stratigrap-hic level during their studies. In this study, Disco-aster multiradiatus Zone is defined in the upperlevel of Thanetian (Table 2).

Tribrachiatus Contortus Zone

Description: Tribrachiatus contortus Zonewas formed between the first and last appearan-ce of Tribrachiatus contortus (Stradner) (Plate,Figure A).

Author: Hay (1964) and Bukry (1973)

Category: Range zone

Stratigraphic level: Early Ypresian

Fossil Assemblage: Coccolithus eopelagicus(Bramlette and Riedel), Discoaster barbadiensis(Tan Sin Hok), Ericsonia ovalis (Black), Fasci-culithus tympaniformis (Hay and Mohler), Towei-us tovae (Perch-Nielsen) and Tribrachiatus con-tortus (Stradner).

Comparison and interpretation: Meriç et al.(1987), Decima et al. (1975), Aydın (2005) defi-ned this zone during their studies. Martini(1971), Toker (1977), Perch and Nielsen (1985a)defined this zone as Marthasterites contortusZone, on the other hand, Okada and Bukry

(1980) and Lang and Wise (1987) defined it asDiscoaster diastypus Zone, Aköz (1981) asMarthasterites tribrachiatus Zone, Wise-Pospic-hal (1990) as Tribrachiatus bramlettei Zone, andBukry (1969) as Marthasterites contortus andDiscoaster diastypus Zone. Perch and Nielsen(1972) did not encounter this zone during theirstudy. In this study Tribrachiatus contortus Zoneis defined in early Ypresian (Table 2).

TEMPERATURE CHANGE OF SEA WATER

In the graphical evaluations based on thenannoplankton species, changes in temperatureof sea water were determined depending on theamount of the nannoplankton species which in-dicate the environments of hot and cold water.According to previous researchers, the numberof Coccolithus eopelagicus is much in moderatesea water (Hay et al., 1967; McIntre et al.,1967,1970; Wei and Wise, 1989; Tantawy, 2003;Villa et al., 2005). Discoaster ve Sphenolithusspecies are represented abundant in moderate-warm water areas (Wei and Wise, 1989; Wiseand Pospichal, 1990; Edwards and Perch-Niel-sen,1975).

As a result of the study, it was determinedthat abundance of Discoaster and Sphenolith isinversely proportional to abundance of Coccolit-hus eoplelagicus.

While the individual number of Coccolithuseopelagicus in the samples in Selandian is 40,that of Sphenolith ve Discoaster is only 3. To-wards the end of Selandian the number of Coc-colithus eoplelagicus decreases, while the num-ber of Sphenolith and Discoaster increases, de-pending on the increasing temperature of thesea water. The number of Coccolithus eoplelagi-cus increases first to 100 and then to 140 to-wards the middle Thanetian while the number ofSphenolith and Discoaster decreased to 3 andthen 2. These data show that the temperature ofthe sea level decreased. Towards the end ofThanetian the individual number of Coccolithuseoplelagicus decreased again to 45 and thenumber of Sphenolith and Discoaster increasedto 38; suggesting that the temperature of the se-

25ULUKIŞLA BASIN NANNOPLANKTON BIOSTRATIGRAPHY


RESULTS

As a result of the nannoplankton biostratig-raphy research on Güney stratigraphic sectionin Ereğli-Ulukışla Basin, five zones, such asFasciculithus tympaniformis Zone, Heliolithuskleinpellii Zone, Heliolithus ridelii Zone, Discoas-ter multiradiatus Zone ve Tribrachiatus contortusZone were determined. Accordingly, it was alsodetermined that the deep sea deposition repre-sented by turbiditic sequence in the basin occur-red between Selandian-Ypresian.

According to the analyses based on the indi-vidual numbers of the nannofossils, it was deter-mined that temperature of the sea level decrea-sed from moderate to warm in Selandian and became cooler in early – middle Thanetian. Bet-ween late Thanetian to Ypresian the temperatu-re again increased and changed from moderateto warm.

ACKNOWLEDGEMENTS

We would like to extend our sincere thanksfrom Dr. Oğuz Ertürk who supported this studyby providing information and contribution, to Ni-hat Bozdoğan (TPAO-Research Center), to Dr.Zühtü Batı, to Nihal Akça and Dr. HayrettinSancay, Mr. Emin N. Eerkan, Ayşegül Aydın(MTA) and to Prof. Dr. Nurettin Sonel (AÜ).

Manuscript received February 23, 2009

REFERENCES

Aköz, Ö., 1981. Karababa Tip Stratigrafi Kesiti’nin (GB Adıyaman) Nannoplankton’ arlaBiyostratigrafik İncelenmesi. AnkaraÜniversitesi Fen Bilimleri Enstitüsü,Yüksek Lisans Tezi 81p. (unpublished).

Aydın, A., 2005. İzmit Kuzeybatısı Geç KratesePaleojen Nannoplankton Biyostratigrafi-si. Ankara Üniversitesi Fen Bilimleri

Figure 4- Nannoplankton zones determined along the Güney stratigraphic section in the study area.

a water increased again. Individual number ofCoccolithus eopelagicus decreased during Ypre-sian and became 30 in middle Ypresian and 5 atthe end of the Ypresian. On the other hand, the

number of Sphenolith and Discoaster increasedand became 42 in middle Ypresian and 43 at theend of the Ypresian. This indicates that the tem-perature of the sea water increased (Figure 4).

Enstitüsü Yüksek Lisans Tezi, 237 p.(unpublished).

Bramlette, M. N. and Sullivan, F., 1961. Cocco-lithophorids and related nannoplanktonof the Early Tertiary in California. Micro-paleontology 7, 129-188.

Bukry, D., 1969. Planktonic Microfossil Biostra-tigraphy of the NW Pasific Ocean.Initial Reports of the Deep Sea DrillingProject 6.79 p.

______, 1973. Low-latitude coccolith biostratig-raphic zonation. Initial Reports of theDeep Sea Drilling Project, 15; 685-703.

Decima, F. R., Roth, P.H and Todesco, L., 1975.Nannoplankton calcareo del Paleocenee dell’ Eocene della Sezione di possag-no: Schweiz. Palaont. Abh., v. 97, 35-161.

Dellaloğlu, A. A., and Aksu, R., 1986. Ereğli(Konya)-Ulukışla-Çiftehan-Çamardı(Niğde) dolayının jeolojisi ve petrol ola-nakları. TPAO. Rapor No.2205 220s.(unpublished).

Demirtaşlı, E., Bilgin, A. Z., Erenler, F., Işılar, S.,Sanlı, D., Selim, N. and Turhan, N.,1973. Bolkardağlarının Jeolojisi: Cum-huriyetin 50. yılı Yerbilimleri Kongresi,Tebliğler, MTA Yayını, Ankara, 608 p.

Dursun, A.İ., 2006. Ereğli-Ulukışla Havzası Ulu-kışla Formasyonunun (Ulukışla ve Çev-resi) Petrol Hazne Kaya Özellikleri. An-kara Üniversitesi Fen Bilimleri EnstitüsüYüksek Lisans Tezi, 68? (unpublished).

Edwards, A.R., Perch and Nielsen, K., 1975.Calcareous nannofossils from the Sout-hern SW Pacific, Deep Sea Drilling Pro-ject Leg 29. Initial Reports of the DSDP,29, 469-539.

Gartner, S. Jr. 1967. Calcareous nannofossilsfrom Neogene of Trinidat, Jamaica andGulf of Mexico. Paleont. Contr. Univ.Kansas. 29, 1-7.

Hay, W.W., 1964. The use of the electron mic-rosroscope in the study of fossils. Annu-al Rep. Smithsonian Inst. (1963); 409-415.

Hay, W.W., Mohler, H.P., Roth, P.H., Schmidt,R.R. and Boudreaux, J.E., 1967. Calca-reous nannoplankton zonation of the

Cenozoic of the Gulf Coast and Carib-bean-Antillean area, and transoceaniccorrelation. Transactions of the Gulf Co-ast Association of Geological Societies,17, 428-480.

Hay, W.W. and Mohler, H. P., 1967. Calcareousnannoplankton from early Tertiary rocksat Pont Labau, France, and Paleocene-Early Eocene correlations. Journ. Pal.,41,6, 1505-1541.

Ketin, İ. and Akarsu, I., 1965. Ulukışla TersiyerHavzasının jeolojik etüdü hakkında Ra-por TPAO Rapor, 339 (unpublished).

Lang T.H. and Wise S. W., 1987. Neogene andPaleocene-Maestrichtian Calcareousnannofossil stratigraphy, Deep Sea Dril-ling Project Sites 604 and 605, Uppercontinental Rise off New Jersey: Sedi-mentation Rates, Hiatuses, and correla-tions with seismic stratigraphy, 661-683.

Martini, E., 1971. Standart Tertiary and Quater-nary calcareous nannoplanktonzonati-on. Proceedings of the 2 nd. PlanktonicConference, 1970, Roma, Edizioni Tac-noscienza,2, 739-785.

McIntre, A.,B, A.W.H and Roche, B., 1967. Mo-dern Coccolithophoridae of the AtlanticOcean. I. Pacoliths and cyrtoliths. DeepSea Res. Oceanogr. 14, 561-597.

______ and Roche, B., 1970. Modern PacificCoccolithophoridae: a paleontologicalthermometer. N. Y. Acad. Sci. Trans.Sre. II 32,6, 720-731.

Meriç, E., Oktay, F. Y., Toker, V., Tansel, İ. andDuru, M., 1987. Adıyaman yöresi ÜstMTA, 2002. 1/500 000 ölçekli jeoloji har-itaları, No: 15 (Adana Paftası). Kretase-Eosen istifinin sedimanter jeolojisi ve bi-yostratigrafisi. Türkiye Jeoloji Bülteni30, 19-32.

Okada H. and Bukry D., 1980. Supplementarymodification and introduction of codenumbers to the low-latitude coccolith bi-ostratigraphic zonation (Bukry 1973,1975) Mar. Micropaleont., 5, 321-325.

Oktay, F. Y., 1982. Ulukışla ve çevresinin stratig-rafisi ve jeolojik evrimi: Türkiye JeolojiKurultayı Bülteni, 25, 15-23.



Pampal, S. and Meriç, E., 1990. Ereğli (Konya)güneybatısındaki Tersiyer yaşlı tortulla-rın stratigrafisi: Türkiye Jeoloji KurultayıBülteni 33,39-45.

Perch-Nielsen, K., 1972. Remarks on late Creta-ceous to Pleistocene coccoliths fromthe North Atlantic: Init. Repts. Deep-Se-a Drilling Project, v. 12, Washington, U.S. Government Printing Office, 1003-1069.

______, 1985a. Mesozoic calcareous nannofos-sils, Eds In Plankton Stratigraphy. Bolli,J. B. Saunders ve K. Perch-Nielsen,Cambridge University Press, 329-426.

______, 1985b. Cenozoic calcareous nannofos-sils, Eds In Plankton

Stratigraphy Bolli, J. B. Saunders ve K. Perch-Nielsen, Cambridge University Pres,472-554.

Sonel, N. and Sarı, A., 2004. Ereğli- Ulukışla(Konya-Niğde) Havzasının Hidrokarbonpotansiyelinin incelenmesi. Gazi Üni-versitesi Mühendislik Mimarlık FakültesiDergisi 19/4, 393-403.

Tantawy, A.A.A.M., 2003. Calcareous nannofos-sil biostratigraphy and paleoecology ofthe Cretaceous-Tertiary transition in thecentral eastern desert of Egypt. MarineMicropaleontology, 47, 323-356.

Toker, V., 1977. Haymana yöresinin (GB Anka-ra), planktonik foraminifera ve nannop-lanktonlarla biyostratigrafik incelenme-si. Ankara Üniversitesi Fen Fakültesi,Doçentlik tezi, 155 p.

Villa, G., Palandri, S. and Wise S.W., 2005.Quaternary calcareous nannofossilsfrom Periantartic implications. MarinePaleontology, 56/ 3-4, 103-121.

Wei, W., 1988. A new tecnique for preparing qu-antitive nannofossil slides. Journal ofPaleontology, 62, 472-473.

______ and Wise, S.W., 1989. Paleogene cal-careous nannofossil magnetobiochro-nology: Results from South AtlanticDSDP site 516. Marine Micropaleonto-logy, 14, 119-152.

Wise, S. W. and Pospichal, J. J., 1990. 37. Pa-leocene to Middle Eocene calcareousnannofossils of ODP sites 689 and 690,Maud Rise, Weddell Sea, 613-638.

PLATE - I

Figure 1- Fasciculithus tympaniformis Hay and Mohler; Sample Number: A 3

Figure 2- Heliolithus kleinpellii Sullivan; Sample Number: A 10

Figure 3a-b- Heliolithus ridelii Bramlette and Sullivan; Sample Number: A 20

Figure 4- Discoaster multiradiatus Bramlette and Riedel; Sample Number: A 33

Figure 5- Tribrachiatus contortus Stradner; Sample Number: A 48

Figure 6- Discoaster saipanensis Bramlette and Riedel; Sample Number: A 46

Figure 7- Tribrachiatus orthostylus Bramlette ve Riedel; Sample Number: A 42

Manolya SINACI ve Vedia TOKER

PLATE - I

INTRODUCTION

Study area is located in a 200 km2 area sur-rounding the Hazar village (Maden town) inEastern Taurus orogenic belt (Figure 1).

When tectonic framework of Turkey is con-sidered, it is located in northeast – southwesttrending East Anatolian Fault zone passing fromsouth of Elazığ, and south of Lake Hazar.Guleman ophiolite was formed after the closure

PETROGRAPHICAL AND GEOCHEMICAL PROPERTIES OF PLAGIOGRANITES AND

GABBROS IN GULEMAN OPHIOLITE

* Ayşe Didem KILIÇ

ABSTRACT.- Petrographical and geochemical properties of gabbros and plagiogranites of Guleman ophioliteare determined. It was concluded that gabbros can be basic rocks on subduction zone and plagioclase rich leu-cocratic rocks (plagiogranite) are differentiation products of fractional crystallization of a basic magma in themagma chamber.

Key words: Neotethys, supra-subduction zone, plagiogranite, gabbros, Taurides.

* Fırat Üniversitesi Mühendislik Fakültesi Jeoloji Mühendisliği Bölümü, Elazığ


Figure 1- Geoylogic map of studied area (Kılıç, 2005)

34 Ayşe Didem KILIÇ

Figure 2- Tectonic units of Turkey and ophiolitic masiffes (changed from Robertson, 2002).

of the Neotethyan ocean as supra-subductionzone ophiolites (Açıkbaş and Baştuğ, 1974;Aktaş and Robertson, 1984; Lytwyn and Casey,1993; Beyarslan and Bingöl, 2000; Parlak et al.,2008; Robertson, 2002; Kılıç, 2005).

The ophiolites have emplaced in five differentzones in Turkey; these are, from south to north,1) Pontide ophiolites, 2) Anatolide ophiolitic belt,3) Tauride ophiolite belt, 4) Southeast Anatolianophiolites, 5) Peri-Arabian ophiolites (Figure 2).All of these ophiolites are the products of sub-duction zone (Robertson, 2002; Göncüoğlu andTurhan, 1984; Floyd et al., 2000).

There are many researches on the geology,petrography, petrology and ore formations of theGuleman ophiolite (Perinçek 1979b; Perinçekand Özkaya, 1981; Özkan,1982; Erdoğan,1982;Özkan, 1984; Bingöl, 1984; Özkan and Öztu-nalı,1984; Sungurlu et al., 1985; Yazgan andChessex, 1991; Kılıç, 2005). The acidic mag-matic rocks (trondheimite, tonalite, diorite, etc.)that take place at the plutonic level of the ophio-lites or at the sheeted dyke complex provide sig-nificant data on the position and origin of the

ophiolites (Hebert and Laurent,1990; Floyd etal., 2000). Formations which do not have vol-canic units such as Guleman ophiolite havegreat significance to understand the tectonicpositions of the ophiolites. Plagiogranites arethe most significant indicators of the arc environ-ments (Floyd et al., 2000). As for the formationof the plagiogranites there are different opinions.It was proposed that, plagiogranites wereformed by the differentiation of a tholeiiticmagma in the Mid-Oceanic Ridge (Coleman andPeterman,1975; Coleman and Donato, 1979;Pallister and Knight, 1981; Floyd et al., 2000), bypartial melting of gabbros (Gerlach et al.,1981;Spulber and Rutherford, 1983; Floyd etal.,2000), and by presence of immiscible liquidsfound together with mafic solutions (Phillpotts,1976; Dixon and Rutherford, 1979; Floyd et al.,(2000).

This paper aims to examine the petrogene-sis, geochemistry and tectonic position of theplagiogranites in Guleman ophiolite, and com-pare their relation to the gabbros. Defining theseproperties is significant for revealing the proper-ties of felsic magmatism.

GEOLOGICAL SETTING

An intensive tectonic activity is observed inthe study area due to presence of big faults suchas the East Anatolian fault and Hazar fault(Figure 1). As for the relation between the litho-logical units, we observe that Guleman ophioliteis thrusted over the Hazar Group, and PütürgeMetamorphics is thrusted over the Gulemanophiolite and Maden Complex. Hazar Group isthrusted over the Maden Complex as well.

From bottom to top, the following units areobserved in the study area (Figure 3): 1) Pütürge Metamorphics, 2) Guleman ophiolite,3) Hazar Group, 4) Maden Complex, 5) Holocenealluviums (Kılıç, 2005).

Pütürge Metamorphics is composed ofPaleozoic-Mesozoic muscovite schists, phyllite,quartzite, calc schist and marbles.

Upper Cretaceous Guleman ophiolite(Erdoğan, 1977; Perinçek and Çelikdemir, 1979)

is composed of two main groups, namely tec-tonites and ultramafic-mafic cumulates.Tectonites are comprised of harzburgite, duniteand podiform chromites in harzburgites. Theultramafic cumulates which have gradual con-tact with tectonites are represented by duniteswith banded or disseminated chromites, wehrliteand clinopyroxenes. A thick layered gabbro leveltakes place on these rocks. It is possible to dif-ferentiate the gabbros as isotope gabbros or asnormal gabbros. Isotropic gabros display aequigranular structure in meso and micro inves-tigations whereas the normal gabbros have larg-er crystals in size. At the upper sections of theisotropic gabbros plagiogranite levels areobserved. Ophiolitic units are cut by isolated dia-base dykes. Since sheeted dyke complex is notpresented in Guleman ophiolite, it is defined asa dismembered ophiolite. Lack of volcanic levelsmay be explained by tectonic stripping or by alater erosion (Parlak et al. 2008). According toÖzkan and Öztunalı (1984), volcanic rocks ofGuleman ophiolite is Caferi Volcanics which are

PLAGIOGRANITES AND GABBROS IN GULEMAN OPHIOLITE 35

Figure 3- Colon section of The Guleman ophiolite (Kılıç, 2005).


stripped tectonically from ophiolite and rested onMaden Complex. Thickness of diabase dykeswhich cut the ophiolitic units at different levels is1 – 1.5 m on average.

Maastrichtian – Lower Eocene Hazar Group(Aktaş and Robertson, 1984) is comprised of anintercalation of conglomerate, sandstone-shale,clayey limestone units.

Middle Eocene Maden Complex is represent-ed by volcanic Karadere Formation (Baştuğ,1976; Sugurlu et al., 1985; Erdoğan, 1977, 1982)and sedimentary Melefan Formation (Açıkbaşand Baştuğ, 1974; Sungurlu et al., 1985) in thestudy area. Karadere Formation is composed ofagglomerate, tuff, volcanic sandstone, andesiteintercalated with mudstone and pillow lava whileMelafan formation is composed of marl, mud-stone, sandstone and grey limestone.

This study aims to study the petrographicaland geochemical properties of gabbros and espe-cially the plagiogranites of Guleman ophiolite andto reveal the character of arc magmatism.

PETROGRAPHY OF GULEMAN OPHIOLITE

Dominant lithology of the Guleman ophioliteis harzburgite. The other rocks are the the man-tle tectonites comprised of podiform chromitelocated in harzburgites and dunites, ultramaficcumulates, gabbros and isolated diabase dykes.The ultramafic cumulates are comprised ofwehrlite, dunite and disseminated or bandedchromites in dunites. On the cumulate level thickgabbro (isotope gabbro, layered gabbro) islocated. Between the two gabbroic level pla-giogranites are observed. Isolated diabasedykes cut the whole succession of Gulemanophiolite at different levels.

Harzburgites constitute 40% of the wholeophiolitic rocks. They are serpentinized at tec-tonic levels and appear as greenish, bright rocksin the field. The main minerals of the harzburgiteare olivine (50-60%), enstatite (50-40%) andchromite (less than 1%). Structural and texturalfeatures such as recrystallization, partial melting

and plastic deformation were preserved in tec-tonites (harzburgites and dunites) (Özkan andÖztunalı, 1984).

Harzburgites and dunites are laterally transi-tive. Dunites display fabric texture and/or granu-lar texture. Their modal mineralogical compo-nents are olivine (90-97%), clinopyroxene (5-2%) and magnetite (5%).

Thick cumulates are observed on the tec-tonite level. The ultramafic cumulates and tec-tonites are laterally transitive. The rocks whichmuch more affected by alteration are wehrliteand clinopyroxene. Wehrlite has mesocumulatetexture and forms clinopyroxene (augite) andplagioclase cumulus minerals; on the otherhand, olivine forms intercumulus minerals. Inter-crystal deformations such as kink banding andplastic flow are not observed. The thick gabbrolayer which overlie the cumulate level is repre-sented by isotope gabbro, normal gabbro andplagiogranites at the upper levels.

Layering in gabbros are defined by thechange of rate of olivine, plagioclase and pyrox-ene in layered gabbros. Isotrope gabbros orequigranular gabbros are the upper section ofthe gabbro level and they have subophitic tex-ture. They are comprised of clinopyroxene (30-35%), olivine (30%) and plagioclase (40-45%).On the other hand, normal gabbros havemesocumulate texture. The most significantproperty that differs isotope gabbros from lay-ered gabbros is the anorthite content in plagio-clases, besides the textural difference(Beccaluva et al., 1994). As a result of micro-scopic study, the anorthite content of plagio-clases is found as 10%.

Plagiogranites are located between the iso-tope gabbros and normal gabbros. These lightcolored acidic rocks can easily be observedingabbros in macroscopic scale. These rockswhich display fine granular texture have a modalmineralogical composition of plagioclase (An20-25) (60-65%), quartz (>20%) and biotite (10-15%) (changed into chlorite) and magnetite.Zoning is observed in the euhedral andsubeuhedral plagioclases in plagiogranites.

Thickness of isolated diabase dykes whchcut the ophiolitic rocks at different levels is 0.5-1m. They display intersertal texture. Modal min-eralogical composition of unaltered diabases isplagioclase (60-80%), clinopyroxene (20-40%)and secondary minerals. Plagioclases have pris-matic shapes. They display albite, albite-carls-bad twinning.

GEOCHEMISTRY

Main oxide and trace element (including rareearth elements) analyses of gabbros (7 sam-ples) and plagiogranites (3 samples) ofGuleman ophiolites were conducted in ACMEAnalytic Laboratories in Canada. Total amountof major oxide and minor elements wereanalysed by ICP-MS method and by acid diges-tion and lithium metaborate/tetraborate fusionmethod on 0.2 gr samples. The results areshown in table 1.

When the results of analyses of the gabbrosand plagiogranites of Guleman ophiolites werestudied in table 1, it was observed that the gab-bros have 48.33-54.88 SiO2, 5.73-11.84 MgO,and the plagiogranites have 60.21-69.19 SiO2and 1.22-2.34 MgO values. LOI values of theserocks are between 1.0 – 4.5 and the rocks dis-play hydrothermal alteration in less amounts.

Gabbros have affected from this alterationeven if less and in mafic element chemistry thiseffect is observed. Due to alteration theNa2O+K2O value is 1.52-4.90%. K2O value isless than that of Na2O. Enrichment of Na mightbe due to spilitization of mafic rocks as a resultof low gade hydrothermal ocean floor metamor-phism.

In AFM diagrams it is observed that somegabbros fall into an area of non-cumulate gab-bro related to arc (Figure 4). This indicates theformation of the primary fraction of solutions indepleted mantle which typicaly occurs at the


Figure 4- AFM diagrams of gabbros (Beard, 1986).


Lihology Plagiogranite Gabbro

Sample No Pl-1 Pl-4 Pl-12 1 2 3 4 5 6 7

SiO2 60.21 69.19 62.52 49.30 53.40 54.88 52.17 48.33 53.77 51.29Al2O3 12.84 13.57 15.56 9.63 14.60 11.56 15.85 12.23 12.56 7.8TiO2 0.71 0.38 1.23 0.70 1.37 1.05 0.46 0.60 1.51 0.47Fe2O3 6.19 3.81 8.24 13.76 9.92 8.42 8.98 12.76 8.24 15.09MnO 0.09 0.08 0.04 0.26 0.13 0.13 0.14 0.16 0.15 0.23MgO 2.34 1.22 1.48 11.66 5.73 6.74 7.22 11.26 6.48 11.84CaO 13.46 3.35 6.03 11.78 6.64 10.84 9.75 11.18 10.42 9.98Na2O 0.19 4.51 3.92 1.46 4.86 3.15 2.85 2.47 3.61 0.51K2O 0.03 0.23 0.34 0.06 0.04 0.66 0.20 0.04 0.06 0.03P2O5 0.07 0.08 0.07 0.07 0.15 0.15 0.04 0.08 0.14 0.07LOI 3.7 3.4 1.0 1.0 2.8 4.1 2.0 1.7 2.9 2.3Total 99.88 99.84 99.43 99.68 99.64 99.92 99.66 99.77 99.81 99.61Mg# 56 55 57 59 49 57 57 54 58 55Rb 0.4 2.6 1.3 <5 1.1 8.2 3.3 3.8 0.5 1Sr 310 166 193 134 115 166 176 122 155 141Y 19 26 30 33.5 32 25.2 15.7 31 27 16.8Zr 45 26 39 18.6 92.7 66.0 25.5 19 51 83.7Nb 1.1 2.8 2.1 0.7 2.1 1.5 0.5 1 1.7 1.4Ba 12 62 73 7 26 69 28 45 32 56Hf 1 1.9 1.3 0.7 2.4 1.8 0.8 1.6 0.9 2.1Ta 0.1 0.2 <0.1 0.1 0.1 <0.1 <0.1 0.1 <0.1 <0.1Pb 0.7 2.6 1.8 0.4 0.3 0.5 0.5 0.3 0.4 0.3Th 0.2 1.1 0.12 1.1 0.7 0.2 0.3 0.6 0.2 0.7U 0.1 0.1 0.1 <0.1 <0.1 <0.1 <0.1 <0.1 <0.1 <0.1La 3.9 4.4 3.83 2.0 2.5 2.3 1.4 2.1 4.1 1.8Yb 1.8 2.61 1.73 0.08 0.13 0.16 0.49 1.01 0.52 2.01Eu/Eu* 0.89 1.13 1.08 0.02 0.02 0.02 0.07 0.02 0.07 0.02(La)N/(Sm)N 0.90 0.95 0.92 0.52 0.78 0.95 0.8 0.75 0.94 0.91

(La)N/(Yb)N 1.04 0.97 1.03 0.46 1 1.14 5.40 1.13 3.28 1.1

Table 1-Major and trace element analysis of the gabbros and plagiogranites of Guleman ophiolite.

floor of the magma chamber of mafic cumulategabbros (Hopson et al., 1981). Plagiogranitesare accepted as a product of a later differentia-tion of such a magma (Hopson et al., 1981).

TiO2 value of the gabbros are between 0.46-1.37 and their Ti content is between 4000-8000ppm which is consistent with the 5000 ppm Ticontent of the island arc tholeiites as indicatedby Pearce and Gale (1977). Low trace elementvalues such as Nb, Y, Zr besides Ti, low Nb/Yamount indicate a subalkaline environment(Floyd and Winchester, 1975, Figure 5).

Clustering of rock samples in Ti/V (<20) areain Ti/1000-V diagram which is one of the discrim-inant diagrams of tectonic environment indicatean island arc tholeiite environment (Figure 6).Similar low Zr amount and low Zr/Y rate (0.5-2.94 in gabbros and 1.0-2.36 in plagiogranites)is typical for island arc (IAT) (Beccaluva et al.,1994; Spulber et al., 1983). When the samplesare in studied in Nb/Th-Y diagram similarly, it isobserved that the rock sampes fall in island arcarea (Figure 7).

The effects of metamorphism observed as aresult of petrographic and chemical analyses,the samples variable in MORB-normalized multi-element spider diagrams and the gabbros vari-able in respect to LILE (Sr, K, Rb, Ba) (Figure 8)reflect ocean flor metamorphism. The most reli-able indicator element in LILE which is affectedby alteration is Th, which indicates enrichment.Th enrichment is an indicator of emplacement ofsubduction zone (Wood et al., 1979; Pearce etal., 1990). In (Nb/Zr)n-Zr diagram, it wasobserved from the distribution of gabbros andplagiogranites that they take place in subductionzone area (Figure 9), and some samples locat-ed out of the area indicate the presence ofprocesses of contamination in evolution of mag-mas (Jenner et al., 1991).

The Th/Y rate, which is the indicator ofenrichment of magma with the solutions sepa-rated from the subductiong plate (Pearce et al.,1990; Edwards et al., 1991) is 0.04-0.012 andthis value is more than MORB (0.03). The low Tiand Zr rates of the samples point out a low melt-ing. Low melting also indicates low crustal thick-


Figure 5- Nb/Y-Zr/TO2*0.0001 diagrams of gabbro (Winchester and Floyd,1975).


Figure 6- Tectonic diagrams of Plajiogranites (circle) and gabbros (trian-gle) (Floyd and Winchester, 10975). OFB: Oceanic FloorBasalts

Figure 7- Nb/Th-Y diagram of gabbro and plagiogranites (Jenner et al., 1991 partlychanged from). Gabbro (triangle), plagiogranite (square).


Figure 8- N-MORB normalized diagram of gabbros.

Figure 9- (Nb/Zr) n-Zr diyagrams of gabbros (triangle) and plagiogranites (sqare).A: Subduction zone volcanic and plutonic area, B: Continent-continentcorossion area. C: Plate interior plutone and lava area, D: Continent-continent collosion peralümina rocks (Jenner et al., 1991)


Figure 10-Rb-Sr diagrams of plagiogranites (Pedersen and Malpas, 1984).

ness (Rheid and Jackson, 1981) and change incomposition of magma is related to interaction ofsubducting plate and mantle, composition ofsubducting plate, enrichment by componentscoming from the mantle, and depletion rate ofmantle. Low concentration of elements comingfrom the mantle such as Nb, Ti, Y and Yb indi-cate a depleted mantle resource.

When trace element contents of the pla-giogranites observed at the upper levels of thegabbros the most conspicuous property is theirlow Rb contents. On Rb/Sr diagram, the wholesamples are below the line which defines the 0.1ratio. This ratio is used by Pedersen and Malpas(1984) for discrimination of the plagiogranitesformed by partial melting and the plagiogranitesformed by fractional crystallization (Figure 10).In all plagiogranites which were assumed tohave formed by differentiation of basic magma

the Rb/Sr is less than 0.1 (Göncüoğlu andTüreli, 1993).

When the rock/chondrite diagram of the gab-bros and plagiogranites of the Guleman ophio-lite was studied, it is seen that the plagiogranitesare richer in Rare Earth Elements (REE) com-pared to gabbros (Figure 11). Observing thegabbros along a rather flat curve compared toplagiogranites can be explained by rather lessdecomposition of the hornblend and/or opaqueminerals (Rao et al., 2004).

In ORG (ocean ridge granites)-normalizeddiagram of plagiogranites (Figure 12) it isobserved that the Nb and Ta values are nega-tive. Besides Nb and Ta, negative values of Euindicate subduction zone (Schilling et al., 1984;McCullough and Gamble, 1991). It is observedthat these rocks have been depleted by high


Figure 11- Normalized diagrams of gabbros (triangle) and plagiogranites (circle).(Sun and McDonough, 1989).

Figure 12- Incompatible elements according to occean ridge granites (fromPearce, 1982).


Figure 13-Gabbros of The Guleman ophiolite. Zr/Nb-Y//Nb (changed from Edwards etal., 1991) and Nb/2-Zr-Y (Mechede, 1986). Plate iunterior mid-plate enrich-ment ((WPE), are enrichment (VYZ.)

fastness elements (HFSE) and enriched in largeion radius elements (LILE). This depletion andenrichment is interpreted as a consequence ofsubduction by Pearce (1982) and Hawkesworthet al. (1977). Another possibility for LILE enrich-ment is the process of contamination (Wilson,1989). Zr/Nb-Y/Nb and Rb/Y-Nb/Y diagrams(Figure 13) define the contamination processes.These data indicate the addition of crust compo-nents to the solution to separated from the sub-ducting slab. Because the negative Eu anomalialso indicate the contamination (Pearce andParkinson, 1993).

In the Rb-Y+Nb diagram prepared for acidicorigin rocks by Pearce (1982) (Figure 14) theplagiogranites take place in volcanic arc granite(VAG) area. The structural position of the gab-bros in the Guleman ophiolite and acidic rockswhich are collected under the name of pla-giogranite, and the Rare Earth element (REE)content show that they have formed by partialmelting of some basic rocks located at the upperlevels of the subduction zone below the islandarc with the effect of the solutions separatedfrom the subducted slab and water (Luchitskayaet al., 2005; Li et al., 1997). The most significant

evidences for the formation by partial melting ofthe basaltic rocks are the depletion of theserocks by Rare Earth Elements (REE), highLa/Yb and Sr values and low Y value.

Therefore, when all the geochemical datawere studied, it is seen that the REE concentra-tions of the gabbros of the Guleman ophiolite is2-9x chondrite and that of the plagiogranites is6-75x chondrite; and they have high REE val-ues. As in Semail (Oman) and Troodos ophio-lites, based on the similarity in REE distribution,it is possible to say these two rock types arecogenetic.

DISCUSSION AND RESULTS

The study area is located in tectonicallymost active region in Turkey. The region has un-dergone many changes by tectonic movementsthat have occurred since the Upper Triassic. The

most significant and relevant to this work is thesubduction process that began with the closureof the Neotethys (Şengör and Yılmaz, 1981; Tüy-süz, 1993) and formation of a wide ophiolitic ba-sin that began to open between the Keban andPütürge massifs (Yazgan, 1984; Yazgan andChessex, 1991). According to these researchers,the Guleman and Kömürhan ophiolites were for-med in this basin and these ophiolites werethrusted over the Arabian platform during Cam-panian. Some researchers indicate that the ophi-olite formation in the region can not be explainedonly by a an oceanic opening (Perinçek and Öz-kaya, 1981; Şengör and Yılmaz, 1981; Aktaş andRobertson, 1984; Turan and Bingöl, 1991). The-se researchers claim that these ophiolites mighthave formed in two different subduction zones.While the Guleman ophiolite has formed in asmall ocean opened between Keban and Pütür-ge Metamorphics, the other ophiolites (e.g. Ko-çali ophiolite) have formed on the oceanic crustlocated between Pütürge and Arabian platform.


Figure 14-Tectonic environment examine diagrasof plagiogranites (interiorspare square) (Pearce ve diğerleri, 1984). ORG: oceanic ridgegranite, VAG: volcanic are granite, WPG: plate interior granite,syn-SCOLG: collision granite


Bingöl (1984) states that Guleman, Kömür-han and İspendere ophiolites, since the UpperTriassic, have formed on an oceanic floor that hasopened between Bitlis-Pütürge massifs with ahigh rate and, since the Upper Cretaceous thisoceanic floor has first broke up to form a subduc-tion northward and as a consequence of this sub-duction Baskil granitoid was formed and by theend of the Upper Cretaceous, Baskil granitoidsand the ophiolites emplaced on the Bitlis-Pütürgemassifs southward. Yılmaz et al. (1992) claimsthat these Late Cretaceous ophiolites (Göksun,Kömürhan, İspendere, Guleman, etc.) are similarin age, lithology and metamorphism and they allformed by the gradual extinction of the southbranch of the Neotethys on the oceanic subducti-on zone dipping northward. Şengör and Yılmaz(1981), Yılmaz et al. (1992), Parlak et al. (2008),Robertson et al. (2007) state that, although theseophiolites display differences in metamorphismgrades, distributions, existence or inexistence ofsheeted dyke complexes and volcanic rocks, theyall have formed as consequences of thrusts du-ring the orogenic movements between Late Cre-taceous and Late Miocene.

Rocks related to Late Cretaceous arca re thebasic, neutral and acidic extrusive and intrusiverocks. While the extrusive rocks were defined as“Elazığ unit” by Robertson et al. (2007) the intru-sive rocks were defined as “Baskil MagmaticRocks” by Aktaş and Robertson (1984) andYazgan (1984) and as“Elazığ Volcanic Complex”by Hempton (1984, 1985) and as “ElazığGranitoid” by Turan and Bingöl (1991) andBeyarslan and Bingöl (2000). The intrusiverocks known as Baskil granitoid are the l-typecalcalkaline rocks that cut the Taurid platform,ophiolites and the extrusive rocks in the north.These rocks are And type active continentalmargin rocks (Yazgan, 1984; Yazgan andChessex,1991; Beyarslan and Bingöl, 2000;Robertson et al., 2007). The gabbros in thestudy area are the extensions of the opholiticseries, their mineralogical and geochemical fea-tures indicate that these gabbros do not belongto Baskil granitoid.

Presence of harzburgites as mantle rocks inGuleman ophiolite and, presence of thick gab-bros with different textural and mineralogicalcomposition, the geochemical features, indicatethat this ophiolite is of “Harxburgitic TypeOphiolite” which is one of the supra-subductionzone ophiolites which developed based on theopening of the upper section of the crust as aresult of the subduction.

As a result of the petrographical and geo-chemical study of the plagioclase-rich leucocraticrocks located at the upper levels of the gabbrosand isotrope gabbros of the Guleman ophiolite, itwas found out that these rocks are products ofisland arc magmatism related to subduction zone.Besides, presence of acidic rocks and location ofthe samples in volcanic arc granitic area (VAG)(Figure 14) indicate island arc activity.

The leucocratic rocks we define under thename of plagiogranite are interpreted to haveformed as a result of the activity in the upper lev-els of the magma chamber (Floyd et al., 2000).Plagiogranites may form by the partial melting(5-15%) of the gabbroic source rocks or by frac-tional crystallization (Floyd et al., 2000).

REFERENCES

Açıkbaş, D. and Baştuğ, C. 1974. Sason-Kozluşarj yöresi jeolojik raporu. Türkiye Pet-rolleri Anonim Ortaklığı Raporu,795s(unpublished).

Aktaş, E. and Robertson, A. H. F., 1984. TheMaden Complex, SE Turkey: Evolutionof the Neotethyan Continental ActiveMargin. In: Dixon, J.E and Robertson,A.H.F.(eds). Geological Evolution of theEastern Mediterranean, The SpecialPublication of Geological SocietyNo:Blackwell Scientific Publication,Edinburg, 375-402.

Baştuğ, C., 1976. Bitlis napının stratigrafisi veGüneydoğu Anadolu sütur zonunun ev-rimi. Yeryuvarı ve İnsan, 1/3, 55-61.

Beard, J. S., 1986. Characteristic mineralogy ofarc-related cumulate gabbros: implicati-ons for the tectonic setting of gabbroicplutons and for andesite genesis, Geo-logy, 14, 848-851.


Beccaluva, L., Coltorti, M., A.,Premti, I., Sacca-ni, E., Siena, F. and Zeda, O., 1994.Mid-ocean ridge and suprasubductionaffinities in the ophiolitic belts of Albani-a. Ofioliti, 19/1, 1-77.

Beyarslan M. and Bingöl, A.F., 2000. Petrology ofa supra-subduction zone ophiolite (Kö-mürhan-Elazığ -Turkey). Canadian Jour-nal of Earth Sciences. 37, 1411-1424.

Bingöl, A. F., 1984. Geology of the Elazığ area inthe Eastern Taurus region: In: Tekeli,O., Göncüoğlu, M. C.(eds). Geology ofthe Taurus Belt, Proceedings of theInternational Symposium. MineralResearch and Exploration Institute ofTurkey (MTA), Ankara, 209-216.

Coleman, R.G. and Peterman, Z.E., 1975.Oceanic plagiogranite. Journal ofGeophysical Research, 80, 1099-1108.

______ and Donato, M. M., 1979. Oceanic pla-giogranite revised. In: Barker, F. (ed).Trondhjemites, dacites, and relatedrocks. Development in Petrology, 6,149-168. Elesevier Scientifics Publicati-on Corporation New York.

Dixon, S. and Rutherford, M. J., 1979.Plagiogranites as late stage immiscibleliquids in ophiolite and mid-ocean ridgesuites: An experimental study. Earth andPlanetary Science Letters, 45, 45-60.

Edwards, C., Menzies, M., and Thirlwall, M.,1991. Evidence from Muriah, Indonesia,for the interplay of supra-subductionzone and intraplate processes in thegenesis of potassic alkaline magmas.Journal of Petrology, Vol.32,No:3, 555-592.

Erdoğan, B., 1977. Geology, geochemistry andgenesis of the sulphide deposits of theErgani-Maden region SE Turkey, Ph. D.Thesis, University of New Brunswick.

______, 1982. Ergani – Maden yöresindekiGüneydoğu Anadolu Ofiyolit Kuşağı’nınJeolojisi ve volkanik kayaları. TürkiyeJeoloji Kurultayı Bülteni, 25, 49-60.

Floyd, P., A., and Winschester, J. A., 1975.Magma type and tectonic setting dis-crimination using immobile elements.

Earth and Planetary Scientific Letters,27, 211-218.

Floyd, R, A., Göncüoğlu, M. C., Winchester, J. A.and Yalınız, M. K., 2000. Geochemicalcharacter and tectonic environment ofNeotethyan ophiolitic fragments andmetabasites in the Central AnatolianCrystalline Complex, Turkey. In: Bozkurt.,E., Winchester, J. A. (eds). Tectonics andMagmatism in Turkey and the surroun-ding area, Geological Society of LondonSpecial Publications, 173, 182-202.

Gerlach, D. C., Leeman, W.P. and Lallement, A.H. G. 1981. Petrology and geoche-mistry in the Canyon Mountain ophioli-te, Orogens Contribution Minerals Pet-rology, 77, 82-92.

Göncüoğlu, M. C. and Turhan, N.,1984. Geo-logy of the Bitlis metamophic belt. In:Tekeli, O. and Göncüoğlu, M. C. (eds).International Symposium on the Geo-logy of the Taurus Belt, Proceedings,237-244.

______, and Türeli, K., 1993. Petrology and ge-odynamic interpretation of plagiograni-tes from the Central Anatolian Ophioli-tes (Aksaray-Turkey). Turkish Journal ofEarth Sciences, 2, 195-203.

Hawkesworth, C. J., O’Nions, R. K., Pankhurst,R. J., Hamilton, P. J. and Evensen, N.M. 1977. A geochemical study of islandarc and back arc tholeiites from theScotia Sea. Earth and PlanetaryScience Letters, 36,2, 253-262.

Hebert, R. and Laurent, R.1990. Mineral chem-istry of the plutonic section of the Troo-dos ophiolite: new constraints for gene-sis of arc-related ophiolites. In: Malpas,J., Moores, E. M., Panayiotou, A., Xe-nophontos, C. (eds). Ophiolites: Ocea-nic crustal analogues. Geological Sur-vey Cyprus, Nicosia, Cyprus, 149-163.

Hempton, M. R., 1984, Results of detailed map-ping near Lake Hazar (eastern TaurusMountains), Geology of the TaurusBelts, 229-235.

______, 1985, Structure and deformation historyof the Bitlis suture near Lake Hazar, so-


utheastern Turkey. Geological SocietyAmerica Bulletin., 96, 233-243.

Hopson, C. A., Mattinson, J. M.,and Pessagno,E. A., 1981, Coast range ophiolite, wes-tern California. In: Ernst, W. G. (ed).The geotectonic development of Califor-nia, Rubey, Vol. I: Englewood Cliffs, Nj,Prentice-Hall, 418-510.

Jenner, G. A., Dunning, G. R., Malpas, J.,Brown, M. and Brace, T., 1991, Bay ofIsland and Little Port complexes, revisit-ed: age, geochemical and isotopic evi-dence confirm suprasubduction-zoneorigin. Canadian Journal of EarthSciences, 28,1635–52.

Kılıç, A. D., 2005. Hazar Gölü (Sivrice-Elazığ)güneyinin petrografik ve petrolojik özel-likleri. Fırat Üniversitesi Fen BilimleriEnstitüsü, Elazığ, Doktora Tezi, 103,(unpublished).

Li, X., Zhou, H., Chung, S., Ding, S., Liu, Y., Lee,C., Ge, W., Zhang, Y. and Zhang, R.,1997. Geochemical and Sm-Nd isotopiccharacteristics of metabasites from cen-tral Hainan Island, South China andtheir tectonic significance. Island Arc,11,129-144.

Luchitskaya, M. V., Morozov, O. L. and Palandz-hyan, S. A., 2005. Plagiogranite mag-matim in the Mesozoic island-arc struc-ture of the Pekulney Ridge, ChukotkaPeninsula, NE Russia. Lithos, 79, 1-2,251-269.

Lytwyn, J. N. and Casey, J. F., 1993. The geoc-hemistry and petrogenesis of volcanicsand sheeted dikes from the Hatay (Kı-zıldağ) ophiolite, southern Turkey: pos-sible formation with the Troodos ophioli-te, Cyprus, along fore-arc spreadingcenters, Tectonophysics, 232, 237-272.

McCullogh, M.T. and Gamble, J. A., 1991, Geoc-hemical and geodynamical constraintson subduction zone magmatism. Earthand Planetary Science Letters, 102,358-374.

Meschede, M., 1986, A method of discriminatingbetween different types of mid-oceanridge basalts and continental tholeiites

with the Nb-Zr-Y diagram. ChemicalGeology, 56, 207-218.

Özkan, Y. Z., 1982. Guleman (Elazığ) ofiyolitininjeolojisi ve petrolojisi. YerbilimleriDergisi, 3-4/6, 33-39.

______, 1984. Guleman ofiyolitinde metamorfiz-ma etkileri. Maden Teknik AramaDergisi 101/102, 47-57.

______, and Öztunalı, Ö., 1984. Petrology of themagmatic rocks of Guleman ophiolite:In: Tekeli, O. and Göncüoğlu, M.C.(eds). Geology of the Taurus Belt,International Symposium Proceedings,Ankara, 285-293.

Pallister, J. S. and Knight, R. J., 1981. Rare-earth element geochemistry of theSamail ophiolite near Ibra, Oman.Journal of Geophysical Research, 86,2673-2697.

Parlak, O., Rızaoğlu, T., Bağcı, U., Karaoğlan, F.and Höck, V., 2008. Geochemistry ofophiolites in the Southeast Anatolia,Turkey. Tectonophysics, doi:10.1016/j.tecto.2008.08.002.

Pearce, J. A.,1982. Trace element characteris-tics of lavas from destructive plateboundaries. In: Thorpe, E. S. (ed).Andesites, Wiley, London, 525-548.

______, ve Gale, G. H., 1977. İdentification ofore deposition environment from traceelement geochemistry of associatedigneous host rocks. Geological SocietyLondon Special Publication, 7, 14-24.

______, and Bender, J.F., de Long, S. E., Kidd,W. S. F.,Low, P. J., Güner, Y., Şaroğlu,F., Yılmaz, Y., Moortbath,S. andMitchell, J.G., 1990. Genesis of the col-lision volcanism in Eastern Anatolia.Turkey. Journal of VolcanologyGeothermal Research, 44,189-229.

______, and Parkinson, I. J., 1993. Trace ele-ment models for mantle melting: appli-cation to volcanic arc petrogenesis.Magmatic Processes and PlateTectonic. Geological Society, 373-403.

Pedersen, R. B., and Malpas, J.,1984. The ori-gin of oceanic plagiogranites from the

49PLAGIOGRANITES AND GABBROS IN GULEMAN OPHIOLITE

Karmoy ophiolite, western Norway.Contributions to Mineralogy andPetrology, 88, 36-52.

Perinçek, D., 1979b. Palu-Karabegan-Elazığ-Sivrice-Malatya alanının jeolojisi vepetrol imkanları. Türkiye PetrolleriAnonim Ortaklığı, Ankara, no: 1361(unpublished).

______, and Çelikdemir, M. E., 1979. Palu-Karabegan-Elazığ-Sivrice-Malatyaalanının jeolojisi ve petrol imkanları.Türkiye Petrolleri Anonim OrtaklığıRaporu (unpublished), 1361.

______, and Özkaya, İ., 1981. Arabistan levhasıkuzey kenarının tektonik evrimi.Hacettepe Üniversitesi YerbilimleriEnstitüsü Bülteni, 8, 91-101.

Phillpotts, A. R., 1976. Silicate liquid immiscibili-ty: Its probable extent and petrogeneticsignificance. American Journal ofSciences, 276, 1147-1177.

Rao, D., R., Rai, H. and Kumar, J., S., 2004.Origin of oceanic plagiogranite in theNidar ophiolitic sequence of easternLadakh, Indıa, Current Science, 87, 7.

Rheid, I. and Jackson, H.R., 1981. Oceanicspreading rate and crustal thicknesses:Marine Geophysical Research, 5, 165-173.

Robertson, A. H. F., 2002. Overview of the gen-esis and emplacement of Mesozoicophiolites in the Eastern MediterraneanTethyan region. Lithos, 65, 1-67.

Robertson, A. H. F., Parlak, O., Rızaoğlu, T.,Ünlügenç, U.C., İnan, N., Taslı,K. andUstaömer, T., 2007. Tectonic Evolutionof the South Tethyan Ocean: Evidencefrom the Eastern Taurus Mountains(Elazığ region, SE Turkey). In: Rıes, A.C., Butler, R. W. H. and Graham, R. H.(eds). Deformation of the ContinentalCrust: The Legacy of Mike Coward. Ge-ological Society, London, Special Publi-cations, Vol. 272, 233-272.

Schiling, G., Vollmer, R., Ogden, J., Kingsley, R.H. and Waggoner, D. G., 1984. Nd andSr isotopes in ultrapotassic volcanicrocks from the Leucite Hills, Wyoming.Contributions to Mineralogy andPetrology, 87, 359-368.

Spulber, S. D. and Rutherford, M. J. 1983. Theorigin of rhyolite and plagiogranite in

oceanic crust: An experimental study.Journal of Petrology,24, 1-25.

Sun, S. S., and McDonough, W. F., 1989.Chemical and isotopic systematics ofoceanic basalts; implications for mantlecomposition and processes. In:Saunders, A. D., and Norry, J. (eds).Magmatism in ocean basins, GeologicalSociety Special Publication, 42, 313-345.

Sungurlu, O., Perinçek, D., Kurt, G., Tuna, E.,Dülger, S., Çelikdemir, E. and Naz, H.,1985. Elazığ-Palu-Hazar alanının jeolo-jisi. Petrol İşleri Genel MüdürlüğüDergisi, 29, 83-191.

Şengör, A.M.C. and Yılmaz, Y., 1981. Tethyanevolution of Turkey; A plate tectonicapproach. Tectonophysics, 75, 181-241.

Turan, M. and Bingöl, A. F., 1991. Kovancılar-Baskil (Elazığ) arası bölgenin tektonos-tratigrafik özellikleri. Çukurova Üniver-sitesi Ahmet Acar SempozyumuBildiriler Kitabı, Adana, 213-227.

Tüysüz, O., 1993. Karadeniz’den OrtaAnadolu’ya bir jeotravers: KuzeyNeotetisin tektonik evrimi. TürkiyePetrolleri Jeoloji Dergisi Bülteni, 5/1, 1-33.

Wilson, M., 1989. Igneous petrogenesis. UnwynHyman, London, 466 s.

Wood, D. A., Joron, J. L., and Trevil, M., 1979. Are-appraisal of the use of trace ele-ments to classify and discriminatebetween magma series erupted in dif-ferent tectonic settings. Earth PlanetaryScientific Letters, Vol. 45, 326-336.

Yazgan, E., 1984. Geodynamic evolution of theeastern Taurus. In: Tekeli, O., Göncüoğ-lu, M. C.(eds). The Geology of the Tau-rus Belt, Proceedings of the İnternatio-nal Symposium, Ankara, 199-208.

______, and Chessex, R., 1991. Geology andtectonic evolution of the SoutheasternTaurides in the region of Malatya. Bulle-tin of Turkish Association of PetroleumGeologists, 3,1-42.

Yılmaz, Y., Yiğitbaş, E., Yıldırım, M. and Genç,Ş. C., 1992. Güneydoğu AnadoluMetamorfik Masiflerinin kökeni. Türkiye9. Petrol Kongresi, Bildiriler, 307-318.

INTRODUCTION

In coastal areas, sandstone weathering iscontrolled by a wide range of factors, such aspetrography of the host rock, wind erosion, exfo-liation, frost and thaw, biological activities andsalt weathering. The impacts of crystallized seasalt on cavity development have been empha-sized by several researchers (Evans, 1970;Mustoe, 1982; Mc Greevy, 1985). As an indurat-ed coastal dune deposit, formed as a result ofcarbonate cementation, eolianite is also a kindof sandstone in petrographic composition and itsmechanism of dissolution and resultant formsbear comparison with the weathered cavitiesthat develop on coastal outcrops of varioussandstones. However, compared to the numer-ous studies on weathering of coastal sandstoneoutcrops, our knowledge of the weathering ofeolianite remains relatively limited.

In this paper, (a) we present two case studiesfrom NW Turkey that shed light on factors con-trolling disintegration of Quaternary eolianite,located on the south coast of Bozcaada Island(lat. 39°48'51'' N to 39°48'42'' N, long. 26°00'12''E to 26°00'26'' E) and (b) Eocene sandstones

outcropping on the west coast of GeliboluPeninsula (lat. 40°19'00'' N to 40°18'58'' N, long.26°12'54'' E to 26°13'10'' E) to contribute to thediscussions on coastal weathering of sand-stones (Figure 1a). For both types of rock, wediscuss the effects of physical disintegrationinduced by crystallization of sea salt, petro-graphic composition, and structural weaknessesbased on field data, thin section interpretationsand several analytical studies.

SITE DESCRIPTIONS

CAPE ZUNGUMA

Bozcaada Island is located 4 km west of theBiga Peninsula (western Turkey) and showsclose geologic and geomorphologic relation-ships with that region. The geology of the island,as described by several authors (Erguvanlı,1955; Kalafatçıoğlu, 1963; Saltık and Saka,1972), consists of several lithologic units thatrange in age from Palaeozoic to Holocene.Palaeozoic metamorphic rocks (marble andschist) and underlying serpentine form the visi-ble basement and are unconformably overlainby conglomerate, limestone and flysch of

COASTAL SALT WEATHERING OF QUATERNARY EOLIANITE (BOZCAADA ISLAND)

AND EOCENE SANDSTONE (GELİBOLU PENINSULA): THE CONTRIBUTION OF

MICROANALYTICAL DATA

Ahmet Evren ERGİNAL* and Beyhan ÖZTÜRK*

ABSTRACT.- In this paper, factors controlling the diverse dissolution of Quaternary eolianite and Eocene sand-stone in two different coastal environments in northwest Turkey were investigated by means of Energy Disper-sive X-Ray Spectroscopy (EDX) coupled with Scanning Electron Microscopy (SEM), X-Ray Diffractometry(XRD), X-Ray Fluorescence Spectroscopy (XRF) analyses and thin section interpretations. With regard to go-verning agents of the weathering process, petrographic attributes, salt crystallization and biological impacts ap-pear to be important. The weathered forms were found to be distinctive in size, shape and the degree of weat-hering owing to different mineral compositions of the host rocks and combined effects of sodium chloride (ha-lite) and calcium sulphide (gypsum) crystallisation during the dry summer period when evaporation conditionsdominate.

Key words: Eolianite, salt weathering, microanalysis, Bozcaada Island, Gelibolu Peninsula, Turkey.

* Çanakkale Onsekiz Mart Üniversitesi, Fen-Edebiyat Fakültesi, Coğrafya Bölümü, Terzioğlu Kampüsü,Çanakkale. [email protected]

Mineral Res. Exp. Bull., 139,51-59, 2009

52 Ahmet Evren ERGİNAL and Beyhan ÖZTÜRK*

Figure 1- (a) Locations of the study sites; (b) oblique aerial photograph of the Cape Zun-guma comprising Quaternary eolianite; (c) Eocene sandstones with honey-comb cavities at Cape Büyükkemikli.

Eocene age. Upper Miocene formations consistof conglomerate, sandstone, claystone, lime-stone and andesite. The western part of theisland is occupied by recent coastal dunes. Inprevious publications, Cape Zunguma (Figure1b), however, was not mapped in detail and waserroneously depicted as composed of Miocenedeposits. A recent study, however, demonstratedthat these outcrops consist of eolianite units ofLate Pleistocene age, based on luminescencedata (Kiyak and Erginal, 2009).

According to climatic data recorded at Boz-caada meteorological station (Geographical co-ordinate: 39°50' N and 26°04'E) for the periodbetween 1975 and 2003, the area receives an-nual average precipitation of 462.5 mm. Maxi-mum and minimum precipitations occur in winter(December: 89.4 mm) and summer (August: 5.5

mm) seasons. The average temperature is 15.4°C. The coldest and the warmest months areFebruary (8.3 °C) and July (23 °C). The island isone of the windiest areas in Turkey. The prevai-ling wind activity is from northeast. The numberof stormy and strong windy days is 86.5 and156.5, respectively.

CAPE BÜYÜKKEMİKLİ

Eocene sandstone crops out at the westernend of the SW-NE-trending Gelibolu Peninsulain the northwestern part of Turkey (Figure 1c).Honeycomb cavities most commonly occur onthe south-facing slope of Cape Büyükkemikli.The geology of the area and its surroundingshas been previously studied by Önem (1974)and Sümengen and Terlemez (1991). TheEocene sandstones with honeycomb cavities

crop out along the 3.3 km-long coastline of CapeBüyükkemikli. Elevations range from sea level to15-20 m at the top of cliffs. Wave-cut platformsthat can be observed about 30 m offshore to thesouth are conspicuously developed on seaward-inclined surfaces of sandstone ledges (Erginalet al., 2007).

In the absence of a meteorological station inthe area studied, data obtained from theGökçeada Meteorological Station (located 14km west of the study area) indicates that thearea receives an average precipitation of 737.9mm per year. Maximum precipitation occurs inNovember, December and January. The amountof monthly average precipitation varies between100 and 140 mm in these months. The areareceives the lowest rainfall in the period fromJune to August, between 11 and 17 mm. Theaverage temperature is 15.1 ºC. The yearly tem-perature range is from 24.6 ºC to 6.7 ºC in sum-mer and winter periods, respectively. The fre-quency distribution and velocity of wind activityis predominantly from NE and SW.

METHODS

Several field surveys were carried out to no-te geo-environmental characteristics of the sitesstudied and to collect samples for analytical exa-mination. Petrography of samples was determi-ned by microscopic examination of thin sections.Energy Dispersive X-Ray Spectroscopy (EDX)and X-ray diffractometry (XRD) were used formajor, minor and trace element characterizationof samples collected. Scanning electron micros-copy (SEM) was performed to characterize mic-ro-porosity, micro-fractures and traces of micro-scale weathering on cavity walls. These analy-ses were performed in the mineralogy, petrog-raphy and technology laboratories of GeneralDirectorate of Mineral Research and Explorati-on, Turkey. To determine chloride ion concentra-tion, the Mohr method (Skoog et al., 2000) wasutilized. Ca, K, Mg and Na concentrations weredetermined by inductively coupled plasma-ato-mic emission spectroscopy (ICP-AES, VarianAxial Libery II Series).

RESULTS AND DISCUSIONS

MORPHOLOGIC CHARACTERISTICS OFWEATHERING FEATURES

Quaternary Eolianite

The eolianite, located on Bozcaada Island,comprises the N30E-aligned Cape Zungumawith a total area of 32120 m2, constituting apromontory some 220 m long, backed by sand-stone and limestone of Miocene age (Figure 1b).Several diagnostic features of this rock, such asforesets having angles between 15° and 20° andabundant content of rhizoliths as organo-sedi-mentary structures, reveal its eolian origin(Kiyak and Erginal, 2009).

Morphologically, the northern coast of thecape is dominated by 2-5 m-high sea-cliffs. Itswestern and southern parts are, however,formed by wave-cut platforms with elevationsbetween 0 and 2 m, where weathered featuresoccur (Erginal, 2008).

Weathered forms are represented mainly bydissolution cavities that display variable physicaldimensions and shapes. In many places, thesecavities are completely or partly occupied by se-a water, thick salt accumulations within them arevery common. From the wave splash zone tonearly horizontal surfaces, cavities occur prefe-rentially on wave-cut platforms (Figure 2 a andb). Because of intensive dissolution, the surfaceof these platforms is quite irregular and markedby the presence of elongated cavities and irre-gular-shape connected pits, which are widespre-ad along structural weaknesses that allow thepenetration of sea water. Both diameters anddepths of the weathered cavities range from afew cm up to over 1 metre. Honeycomb-likeforms are absent.

Eocene sandstone

Weathering forms on the Eocene sandstonesare characterized by the common presence ofhoneycomb cells (Figure 1c). Along the wave-splash zone (0-1 m) on the surface of dipping

BOZCAADA QUATERNARY EOLINITE 53


Figure 2- (a) View of numerous weathered cavities on wave-cut platforms; (b) a closer view of a cavity occu-pied by sea salt precipitates.

planes with N60ºE trend and 37º dip, the lengthsof honeycomb cells range from 15 to 65 mm,widths from 15 to 50 mm, and depths from 10 to45 mm (Erginal et al., 2007). Although they havecircular or joint-controlled ellipsoidal shapes ingeneral, the walls of cells are partly irregular dueto the activities of rock barnacles, such asSemibalanus balanoides (Linnaeus 1758) andthe gastropod Littorina neritoides (Linnaeus1758).

In some places, larger cell sizes (length: 3.5cm-10 cm, width: 2.5 cm-8 cm, and depth: 1.5cm-6 cm) are present, likely related to the moreabundant presence of rock barnacles. Thesebioeroders, especially Balanus populations, set-tled on southwest faces or in the bottoms of cav-ities conforming to east-west trending fractures.Closely spaced cells with sharp wall boundariesare well developed as a result of the enlarge-ment of cavities through bioerosion of cavitywalls. SEM analysis demonstrates that Balanusplays a significant biologic role in the weatheringof the rock. Figure 3a shows evidence of thisbio-erosion by the abundance of rock fragmentssurrounding the organism. It was also observedthat the surfaces inhabited by Balanus aremarked by shallow holes where traces of bothchemical weathering and physical disintegrationare present (Figure 3b).

MICRO-ANALYTICAL RESULTS RELATINGTO SALT WEATHERING

Quaternary Eolianite

Thin section analyses show that the studiedeolianite is lithic arenite in composition accord-ing to the classification of Pettijohn et al. (1987).The rock consists mainly of fragments of quartz,plagioclase, orthoclase, and, in lesser amounts,microcline, epidote, chloride and leucoxene.These mineral fragments constitute 40% of thepetrographic composition. Several angular rockfragments such as quartzite, schist, micritic lime-stone, various magmatic rocks and microfossilsare also found that make up the other 60%.Limestone fragments are predominant. All thesecomponents are found together by sparitic cal-cite and meniscus cements.

XRD data (Figure 4a) also demonstrated thewidespread presence of calcite and quartz with-in the rock. The weathering residue depositedwithin cavity bottoms yields main peaks ofquartz, calcite and, to a lesser amount, otheraccessory minerals such as rutile (Figure 4b).However, other minerals detected in thin sec-tions were not identified in the XRD diffrac-tograms, which reveal that the weathering of therock is widely associated with dissolution of Ca.


Figure 4- XRD diffractograms of eolianite (a) and its weathered pro-duct (b).

Figure 3- SEM images of Eocene sandstones; (a) weathered residues around, and (b) underneath a cavitycaused by the rock barnacle Semibalanus balanoides.

56 Ahmet Evren ERGİNAL and Beyhan ÖZTÜRK

Figure 5- SEM images of eolianite; (a) the interface between salt crust and eolianite; (b) halite and gypsum crys-tals occupying micropores.

According to ICP-AES analysis, salt samplesextracted from cavity bottoms contain Ca (3.546ppm), K (12.450 ppm), Mg (7.942 ppm), Na(358.607 ppm). The Mohr method (Skoog et al.,2000), used to determine chloride ion concen-tration, revealed that Cl is found in an amount of570 ppm. Based on these values, the analyzedsalt is composed of NaCl (91 %), KCl (2.4 %),CaCl2 (0.98 %) and MgCl2 (3.3 %). The predom-inance of halite (NaCl) is confirmed by the EDXdata, which also showed the existence of gyp-sum (CaSO4.2H2O). Thus, physical disintegra-tion of eolianite is closely associated with thecombination of halite and gypsum, as confirmedby SEM images (Figure 5a and b), showing aprecipitated thick (max. 1 mm) salt crust over therock surface and within micro-cavities. Theseobservations indicate that the combined effectsof halite and gypsum precipitated by the evapo-ration of sea water play an important role on thephysical disintegration of eolianite in the studyarea, as previously emphasized elsewhere byGoudie et al., (1997), Goudie and Viles (1997)and Robinson and Williams (2000).

Eocene sandstones

To make a comparison with eolianite weath-ering, salt weathering on the surface of sand-stone beds exposed on the Gelibolu coast wasstudied. The sandstone unit, underlain by silt-stones with thin or laminated bedding features,is a yellow, fine-grained, calcite-cemented, mod-erately-sorted sub-greywacke according to Folket al. (1970) classification. It is made up of pre-dominantly quartz and plagioclase with traceamounts of biotite and muscovite. Lithoclasts ofserpentine, chert and metamorphic rocks arealso abundant. Beds are generally a few cm to50 cm thick and dip from 30° to 50° toward thesoutheast. Honeycomb type of weathering ispredominant (Erginal et al., 2007).

Salt crystallization induced by wind-enhan-ced evaporation of saline solutions deposited bysea spray is significant in development of ho-neycomb weathering in the coastal environment,as pointed out by several researchers (Mustoe,1982; Matsukura and Matsuoka, 1991; Rodrigu-es-Navarro et al., 1999; McBride and Picard,

2004). EDX analyses carried out on salt samp-les collected from the honeycomb cells in Au-gust 2008, the driest period in this study area,demonstrated Na and Cl as the main constitu-ents of the composition with total amounts of39.31 % and 60.69 %, respectively. However,another sample yielded a more complex mixturecomprising O (47.24%), Na (1.04%), S(22.46%), Cl (0.73%) and Ca (28.53%), sugges-ting the composition of gypsum (CaSO4.2H2O).Thus, it can be stated that salt precipitations in-volve both halite and gypsum, similar to thoseseen in the weathered eolianite.

SEM images (Figures 6 a and b) demon-strate the shapes and dimensions of halite andgypsum crystals. The salt encrustations withmaximum thickness of 100Ìm were composed ofcubic crystals of halite with sizes between 10 Ìmand 30 Ìm (Figure 6a). The interfaces betweensalt encrustations and the sandstone body arecommonly voided and most of the voids areoccupied by salt crystals. The cube-shapedcrystals of halite are also covered with prismaticgypsum crystals, connected to each other withthin filament-like forms. The chain– shaped cir-

cular structures formed by halite crystals (Figure6b) appear to coat the walls of weathering cells,which suggests that physical disintegration cau-sed by pressure of crystallized salt within themicro-pores of the host rock is the most com-mon mechanism of salt weathering (Evans,1970; Bradley et al., 1978; Mustoe, 1982; McGreevy, 1985).

CONCLUSIONS

This study demonstrates that the Quaternaryeolianites and Eocene sandstones from thestudy area exhibit significantly different coastalweathering features. In particular, the Eoceneunits are characterized by honeycomb weather-ing cells whereas the Quaternary eolianites lackhoneycomb cells but display abundant, largerbut more heterogeneous dissolution cavities,many of which have exploited structural weak-nesses within the rock.

Precipitation of halite and gypsum from pen-etrating salt-spray appears to be the principalagent of destructive weathering in both types ofdeposit but physical bioerosion by molluscs


Figure 6- SEM images showing coastal salt weathering on Eocene sandstones; (a) the interface between saltcrust (top) and sandstone; (b) arcuate arrangement of halite crystals on the wall of a honeycomb celldeveloped in micropores within sandstone.


(barnacles and gastropods) is also important inenlarging chemically formed cells, especially inthe Eocene sandstones. In contrast, the close-spaced strata and cross-bed planes that charac-terize the eolianites favour leeward-drainage ofimpacting sea-water and saline spray. This fea-ture, together with the higher carbonate contentof the eolianites, leads to large-scale dissolutionand rapid enlargement of weathering cavities inthese Quaternary units.

ACKNOWLEDGEMENTS

We thank Dr. Yusuf Dilgin for his help withdetermination of chloride ion concentrationusing the Mohr method. Dr. Okan Zimitlioğlu isthanked for painstaking efforts in thin sectionstudies and EDX/SEM analyses. This paper wassupported by Çanakkale Onsekiz MartUniversity Research Foundation (Project num-ber: 2008/32).

Manuscript received February 2, 2009

REFERENCES

Bradley, V.C., Hutton, J.T. and Twidale, C.R.1978. Role of salts in development ofgranitic tafoni, South Australia. Journalof Geology, 86, 647-654.

Erginal, A.E., 2008. Coğrafya ve Jeoloji Labora-tuarı Bozcaada: Keşfedilmemiş Yerbi-limsel Değerler. Bozcaada DeğerleriSempozyumu, 25-26 Ağustos 2008,Bozcaada, s: 173-181 (in Turkish).

Erginal, A. E., Gönüz, A., Bozcu, M., Ateş, A..S.and Çetiner, Z.S., 2007. The first fin-dings on the origin of alveolar disinteg-ration at the western shores of GeliboluPeninsula. Bulletin of the Mineral Rese-arch and Exploration, 134: 27-41.

Erguvanlı, K. 1955. Etüde Geologigue de l'ile deBozcaada. Bulletin de la Société Géolo-gique de France, 6, 399–401.

Evans, I.S. 1970. Salt crystallization and rockweathering: A review. Revue deGéomorphologie Dynamique, 19, 153-177.

Folk, R.L., Andrews, P.B. and Lewis, D.W. 1970.Detrital sedimentary rock classificationand nomenclature for use in New Ze-land. New Zeland Journal of Geologyand Geophysics 13, p. 955.

Goudie AS. and Viles H.A. 1997. Salt Weathe-ring Hazards, Wiley: Chichester.

______, Viles, H.A. and Parker, A.G. 1997. Mo-nitoring of rapid salt weathering in thecentral Nabib Desert using limestoneblocks. Journal of Arid Environments,37, 581-598.

Kalafatçıoğlu, A. 1963. Ezine civarının ve Boz-caada'nın jeolojisi, kalker ve serpantin-lerinin yaşı. MTA Dergisi 60, 60-69 (inTurkish).

Kıyak, N.G. and Erginal, A.E., 2009. A Geomorp-hological and Optical Stimulated Lumi-nescence Dating Study of Eolianite onthe Island of Bozcaada, Turkey: Prelimi-nary Results. Journal of Coastal Rese-arch (submitted to journal).

Matsukura, Y. and Matsuoka, N. 1991. Rates oftafoni weathering on uplifted shore plat-forms in Nojima-Zaki, Boso Peninsula,Japan. Earth Surface Processes andLandforms, 16, 51-56.

Mc Bride, E.F. and Picard, M.D. 2004. Origin ofhoneycombs and related weatheringforms in Oligocene Macigno Sandstone,Tuscan Coasts near Livorno, Italy. EarthSurface Processes and Landforms, 29,713-735.

Mc Greevy, J.P. 1985. A preliminary scanningelectron microscope study of honey-comb weathering of sandstone in a co-astal environment. Earth Surface Pro-cesses and Landforms, 10, 509-518.

Mustoe, G.E. 1982. The origin of honeycombweathering. Geological Society of Ame-rica Bulletin, 93, 108-115.

Önem, Y. 1974. Gelibolu ve Çanakkale dolayla-rının jeolojisi. TPAO (Turkish PetroleumCorporation) Report no. 877 (in Turkish,unpublished report).

Pettijohn, F.J., Potter, P.E. and Siever, R. 1987.Sand and Sandstone. Springer &Verlag,Berlin, 553 p.

Rodriguez-Navarro, C., Doehne, E. and Sebas-tian, E. 1999. Origins of honeycomb we-athering: The role of salts and wind. Ge-ological Society of America Bulletin,111, 1250-1255.

Robinson, D. and Williams, R.B.G. 2000. Experi-mental weathering of sandstone by com-binations of salts. Earth Surface Proces-ses and Landforms, 25, 1309-1315.

Saltık O. and Saka, K. 1972. Saros Körfezi ku-zeyi, Gelibolu Yarımadası, İmroz-Boz-

caada ve Çanakkale sahil şeridi jeolojiincelemesi: TPAO Rapor No; 786 (inTurkish).

Skoog, D.A., West, D.M., Holler, F.J. and Cro-uch, S.R. 2000. Analytical chemistry: Anintroduction, 7th edition). New York: Sa-unders College Publishers.

Sümengen, M. and Terlemez, İ. 1991. Güneyba-tı Trakya yöresi Eosen çökellerinin stra-tigrafisi. MTA Dergisi, 113, 17-30 (in Tur-kish with English abstract).


INTRODUCTION

Zeolites which are defined as hydrous alim-inium silicates with alkaline and earth alkalineelements are among significant industrial rawmaterials because of their physical and chemi-cal properties.

In this study the zeolite samples collectedfrom İzmir (Foça), Balıkesir (Bigadiç) andManisa (Gördes) regions were investigated fortheir mineralogical and technological propertiesto define their areas of usage (Figure 1).

For this reason, thin sections of the sampleswere prepared and their mineralogical determi-nations, XRD and XRF analyses were per-formed. By thin sections and XRD analysestypes of zeolites were determined. As for thetechnological properties, pre-technologicalinvestigation methods, water and oil absorptioncapacities, cat litter test, whiteness and abrasiontests, porosity and pozzolanic tests were appliedto reach to the results of the areas of usage.Experiments and tests were conducted in thelaboratories of the Department of MAT of MTA.

MINERALOGICAL AND TECHNOLOGICAL PROPERTIES OF THE ZEOLITES FROM

FOÇA (İZMİR), BİGADİÇ (BALIKESİR) AND GÖRDES (MANİSA)

Günnur ULUSOY* and Mustafa ALBAYRAK**

ABSTRACT.- Technological analyses of zeolites are important for their areas of use. Zeolite samples were col-lected from different regions (İzmir-Foça, Balıkesir-Bigadiç, Manisa-Gördes) for this study. First mineralogical and chemical analyses of the samples were conducted in the study. Later on, technologicaltests of the samples were made for their utilizing in ceramic industry (pre- technological), in paper industry (fill-ing and coating) and as cat litter. Finally the results were evaluated. It was concluded that some samples can be used in baked ceramics in ceramic industry; they have high whiten-ing properties to be used in paper industry. As for cement additives, their flexural strength is observed in a rangebetween 0,94 - 12,85 kgf/cm2 while their compressive strength is between 2,08 - 51,20 kgf/cm2. Porosity ofsome samples are above 40% which means they meet the criteria to be used as soil conditioners.

Key words: Zeolite, Foça, Bigadiç, Gördes

* Maden Tetkik ve Arama Genel Müdürlüğü,Maden Analizleri ve Teknolojisi DairesiBaşkanlığı,06520 Ankara [email protected]**Maden Tetkik ve Arama Genel Müdürlüğü,Maden Analizleri ve Teknolojisi DairesiBaşkanlığı,06520 Ankara [email protected]


Figure 1- Location map of the study area(Foça,Bigadiç and Gördes)

62 Günnur ULUSOY and Mustafa ALBAYRAK

Figure 2- Geological map of Bigadiç and its surroun-dings and sampling locations (modifiedfrom Ercan et al., 1984).

Literally the word “ZEOLITE” means “boilingrock”. The name was given to the rock since itexplodes and decomposes when heated. Ingeneral, the natural zeolites are used as lightbuilding rocks and light aggregates in construc-tion industry and as additives in paper industryand as soil conditioner and additive for fertilizersin agriculture industry (Yücel, 1987).

Zeolite minerals include empty spaces andchannels in their structures. Since they can losethe water in these empty spaces and channelswithout changing their structures under hightemperatures, based on their loose skeletalstructures, they have replaceable cations. Forthis reason, they are succesfully used in adsorb-tion, ion Exchange and dehydration areas.

Öner et al., (2000) have studied differentaspects of the zeolites collected from Manisa-Gördes area in course of their project titled“Geological, mineralogical and chemical proper-ties of zeolitic tuffs and their areas of usage inindustry”.

Albayrak et al., (2001) have used zeolite(clinoptilolite) instead of quartzite to produce gasconcrete during their Project titled “Production oflight building Stones from zeolites”.

Kalafatoğlu et al., (2002) prepared “Bibliog-raphy of Zeolite Research” in TÜBİTAK Marma-ra Research Center in which, researches on ze-olites in Turkey based on earthsciences; rese-arches on characterization of zeolites in Turkey;application-oriented researches on zeolites,synthetic zeolites and zeolitic borophosphateswere discussed.

GEOLOGY

MANİSA GÖRDES REGİON

The volcanosedimentary formations knownas Gördes zeolites were formed by flowing anddeposition of rhyolitic, rhyo - dacitic eruptions ofKobaklar Volcanism (Göktaş et al., 1996) locat-

ed in the north of Gördes into the Lake Gördeswhich was a sedimentation basin in that period.

In Gördes and the surrounding area, meta-morphic rocks (gneiss, migmatite, micaschist,quartzite) of Menderes massif are located at thebasement (Figure 2).

Lower Miocene Kürtköyü, Yeniköy and Çıtakformations unconformably overlie the Menderesmassif. Kürtköyü formation is dominantly com-posed of boulderstone, coarse conglomerate,conglomerate and sandstones. It is uncon-formably overlain by Yeniköy formation which iscomprised dominantly of conglomerate, sand-stone and mudstones which includes lignite lev-els. There are algal limestone interbeds at theupper levels of this formation.

ZEOLITES OF İZMİR-BALIKESİR - MANİSA REGION 63

Küçükderbent formation conformably andtransitively overlies the Yeniköy formation. It isdominantly comprised of clayey limestone,shale, mudstone, sandstone, tuff and less bitu-minous shales which reflect a lacustrine environ-ment. This unit is unconformably overlain byGökyar formation which is made up of rhyolitictuffs. In Manisa-Gördes region mostly clinoptiloliteminerals and less hoylandite and analcime bear-ing levels are observed (Vural and Albayrak,2005). Calcalkaline volcanism comprised of lavaand tuffs of dacitic, rhyodacitic compositionwhich activated in Early Upper Miocene endsthe Küçükderbent lacustrine deposition. Thesevolcanics were defined as KaraboldereVolcanics (Ercan, 1983). All these units wereunconformably overlain by Upper Miocene-Pliocene sedimentary sequence.

BALIKESİR (BİGADİÇ) REGION

The sequences cropping out in Balıkesir-Bigadiç region were compiled from Ercan et al.,(1984a, b) (Figure 3).

The Lower Miocene Dedetepe formation iscomprised of dacite, rhyodacite, rhyolite, tuff andagglomerate. At the lower levels of the formationbrown, pink, grey colored, locally altered dacite,rhyolite and agglomerates take place, on theother hand, at the upper levels tuffs are domi-nant. The Çandağ basalt which is located on theunit is comprised of basalt, trachy - basalt,agglomerate and tuffs, from bottom to top. Thefresh surfaces of the rocks are black coloredwhile the altered parts are red-brown. The unit isquite hard and irregular. Flow structures andhexagonal cooling (columnar jointings) struc-tures are observed in the lavas. On these vol-canic rocks unconformable lacustrine depositsknown as Bigadiç formation are observed. Thisformation is comprised of five members. Theseare: Güvemçetmi Limestone Member, Akçakertiltuffite member, Yeniköy limestone member, Be-ğendikler tuffite member, İskele LimestoneMember. Bigadiç formation is probably of UpperMiocene-Lower Pliocene age. Akçakertil tuffitemember which conformably overlies the Güvem-çetmi limestone member in the study area is qui-te widespread, its tuffite levels are light grey,white, yellowish in color and they are dacitic andrhyodacitic in composition. It is locally calciteand silicium cemented. Tuffs are also observedin Akçakertil tuffite member. The tuffs which areintercalated with tuffs have various grain size,they are glassy and irregularly distributed.Ataman (1977) determined zeolite formations inthese tuffs. Beğendikler tuffite member is coarsegrained in general, however fine grains also canbe observed. It is formed by deposition of rhy-olitic glassy tuffs in a lacustrine environment.The coarse grained and porous, thick tuffites arelocated at lower levels but fine grained glassytuffites are observed in the upper levels. Theselevels also include zeolite (clinoptylolite) forma-tions as Akçakertil tuffite member does. Theyoungest units in the study area are unconsoli-dated or less consolidated alluviums. Alluviumsare mostly observed along Simav stream and inBigadiç plain.

Figure 3- Geological columnar section of Gördesand the surrounding area (modified fromGöktaş, 1966).


FOÇA-İZMİR REGION

In Foça region Miocene and younger unitscrop out. Stratigraphically andesite, basalt, rhy-olite, dacite, tuff and agglomerates overlie con-glomerate, sandstone, siltstone, claystone andmarly sequence. At the upper levels dirty white,beige colored limestones take place. Alluviumsare mostly in form of loosely consolidatedblocks, pebbles, sand, silt and clay intercala-tions (Lengeranlı et al., 1998).

In Foça-İzmir region, the apparent + proba-ble reserve with high clinoptilolite content isabout 120 million tons (Esenli, 2002).

During the research carried out by MTA, besidesclinoptilolite, presence of hoylandite and mordeniteminerals were determined (Albayrak, 2008).

EXPERIMENTAL STUDIES

During the research, experimental studieswere carried out on the areas of usage for thezeolites (clinoptilolite) collected from Foça,Bigadiç and Gördes regions. First, the chemicaland mineralogical analyses of the samples wereconducted. Second, pre-technological tests(original position and color, baking condition andcolor, reaction with dilute acid, dispersion inwater, plasticity) and tests for usage in paperindustry as filling and coating materials, andusage in cement industry and cat litter were per-formed.

TESTS APPLIED AND APPLICATION

STAGES

1. Drying.- This is the process of drying of thesamples at 105 °C in drying ovens before weighbridge.

2. Grinding.- This is the process of grinding ofthe samples in ball mill until the desired grainsize is reached.

3. Pre-Technology Observation Tests asCeramic Raw Material

a- Original color and condition.- Expressesthe original color and condition of the sample(crushed or as particles).

b- Dispersion in water.- Shows whether apart of the material is dispersed or not in thewater.

c- Plasticity.- A small part of the crushedmaterial is mixed with water and plasticity isexamined by hand.

d- Reaction with dilute acid.- 10% dilute HClis dripped on the sample to see whether thesample foams or not. If foaming is observed, thsis due to presence of carbonaceous material.

e- Baking condition and color.- Baking condi-tions and colors are observed at 1150 °C, 1300°C, 1430 °C.

4. Water Absorption (for samples as parti-cles) Test.- This test is conducted according to“TS699 January 1987” standard.

5. Oil Absorption Test.- This test is conductedaccording to “TS 2583 EN ISO 787 – 5 /December 1997” standard.

6. Cat Litter Test.- This test is conductedaccording to “TS 12131 / February 1997” stan-dard.

7. Whiteness Test.- This test is conductedaccording to “TS 12131 / February 1997”Standard under Canadian Research Institute,Model CG – 166 reflectometer using green fitler.

8. Abrasion Test: - This test is conducted ac-cording to “TS 10521 / December 1992” stan-dard using the “Voith Allis Valley LaboratoryEquipment” at 6000 revolution.

9. Porosity Test.- This test is conductedaccording to “TS 699 January 1987” standard.

10. Pozzolanic Cement Test.- This test isconducted according to “TS 25 / April 1975”standard.

Tests were conducted at laboratories ofDepartment of MAT. Mineralogical determina-


Table 1- Sampling locations, coordinates and sample numbers.

tions of the samples were carried out inMineralogy and Petrography Unit. Chemicalproperties of the samples were determined atAnalytical Chemistry Unit. Thechnological prop-erties, on the other hand, were determined in the

laboratories of the Industrial Raw Materials andCeramic Materials Research Unit.

Sample numbers, sampling locations, coordi-nates, 1: 100 000 scale topographical map num-bers are given in table 1.

MINERALOGY

XRD analyses results of the samples aregiven in table 2. According to these results, it isobserved that the samples in general includeclinoptilolite and hoylandite minerals as well asglassy materials, quartz, opal and illite andsmectite group clay minerals. Minerals are givenin table 2 according to abundance in the rock.

It was observed also that, the dominant min-erals in the samples from İzmir-Foça region arehoylandite, in contrast, the samples collectedfrom Balıkesir-Bigadiç and Manisa-Gördesclinoptilolite mineral is more dominant.

GEOCHEMISTRY

Results of the chemical analyses of the sam-ples collected from Balıkesir, İzmir and Manisaregions and their density values are given intable 3. It is observed that SiO2 values of thesamples are equal to or higher than 70% andAl2O3 values are higher than 10% for all thesamples. Density values of the samples varybetween 1.98 and 2.40, and fire loss values arebetween 3.40 and 9.65.


Table 2- Mineralogical descriptions of the samples based on XRD analyses.

Table 3- Results of chemical analyses of the samples and their density values


DETERMINATION OF AREAS OF USAGEOF ZEOLITE

RESULTS OF PRE-TECHNOLOGY TESTSAS RAW MATERIAL

Pre-technological examination of the sam-ples for ceramic were carried out and the resultsare given in table 4. Water disperssion test ofthe samples is the control whether a small partof the sample disperses in the water or not. Thebehaviour of the sampe gives an idea about thegrain size and decreases the grinding cost of asample which can easily disperse in the water.However, no dispersion in the samples wereobserved (Table 4).

The crushed samples were mixed with somewater and plasticity is examined by hand. Afterthe test, it was observed that the plasticity isvery little or none for the samples. Therefore,they can be used after mixing with some materi-als with high plasticity. The acid reaction of thesamples is made by pouring some dilute acid

drips on the sample and carbonate content ofthe samples is observed consequently.

Presence of carbonate causes cracks duringand after baking. Fort his reason, materials con-taining carbonates are not good for ceramics.The results of the tests carried out by 10% HClis given in table 4.

During the baking tests, the materials werebaked at 1150 °C -1300 °C -1430 °C to see theircolors. Figure 4 shows the colors of the samplesafter baking test and table 4 shows the colorsand conditions after the test.

According to the results of the chemicalanalyses (Table 3), the Al2O3 content is too lowto be used in ceramic industry, however, the per-centage of the color providing oxides, Fe2O3and TiO2 are between the limits according to TS5396/December 1987 standards.

Consequently, these zeolites can be takeninto consideration to be used in ceramic industryat certain percentages together with kaolin.

Figure 4- Baking conditions and colors of the samples (1150 °C ).


Table 4- Ceiramic pre-technological evaluation of the samples


WATER ABSORPTION TEST AS PARTICLES

Water absorption tests of the samples wereconducted according to “TS 699 January 1987Natural Building Stones Inspection and TestMethods” and the results are given in table 5.

CAT LITTER TEST

The prerequisite for the samples to be usedas cat litter is to define mudding in the samples.An amount of the sampe is left in the still water.In case the sample is dispersed in the water, thewater absorption test is not conducted and the

sample is recorded as not suitable to be used ascat litter. If no mudding is observed, waterabsorption test is applied. When the results areevaluated according to table 6, since the waterabsorption value is low, we can think that thesamples can anly be used after being mixedsome highly absorbent materials.

WHITENESS, ABRASION AND OILABSORPTION TESTS

In paper production, many industrial rawmaterials, mainly calcite and zeolite are being

Table 5- Water absorption values of the samples.


Tablo 6- Cat litter water absorption values.

Table 7- Whiteness / abrasion values according to TS 10521 and TS11653 standard

used. These materials are also being used asfilling and coating materials.

The minerals used as filling materials areused to increase the opacity and softness of thepaper, and when added to whitened paper, theyare useful in increasing the whiteness of thepaper, and absorption of the ink in the paper andconsequently to increase the printing quality.

Therefore, among the features expected froman ideal filling material, higher whiteness, graindistribution, high immersion in the pulp, non-dis-persion in the water, low hardness (abrasion)and cheapness from economical point of viewcan be counted. For this reason, abrasion,whiteness and oil absorption tests were made tosee the usage of the samples in paper industry,(Table 7).


When we evaluate the results of the white-ness and abrasion tests of the samples, we seethat, when the values indicated in (TS10521,TS11653) standards, the whiteness values ofthe samples FO-20, FO-35 and KIR-3 areobserved to be at usable limits. In this case, thesample FO-20 can be used for filling purposesaccording to TS 10521 and TS 11653 and thesample FO-35 can be used as filling materialaccording to TS 10531 and as filling materialaccording to TS 10521.

The abrasion values are above the valuesindicated in the standards, therefore the sam-ples are considered as not suitable.

In general, as a result of the examination forthe purposes of paper industry, the whitenesspercentage of the samples FO-35 and KIR-3 aresuitable to be used as filling material. The highabrasion index requires low additives withrespect to the paper quality used for filling.

According to table 8, in order to make anevaluation for oil absorption characteristics, itmust be compared with another material ofwhich oil absorption value is known.

POROSITY TESTS

For porosity tests, the samples were drieduntil fixed weighing at 105±5 °C and then theirporosities and unit voluminar weights weredetermined accordding to TS 699 January 1987standards (Table 9). The porosity values of thesamples are observed to be high.

According to the regulations published in“official newspaper” dated and numbered of04.05.2004, 25452 about the Production,Exportation, Importation and market supply ofthe Organic, Organomineral Soil Conditionersincluding special microbial and enzymes, theporosity value must be 40% minimum to use assoil conditioner.

Table 8- Whiteness – abrasion – oil absorption values of the samples.


Table 9- Unit voluminar weight and porosity percentage of the samples.

The research conducted by us is based onthis regulation, and the porosity test resultsshow that the sample B-6 complies with therequirements of the above mentioned regulationand can be used as soil conditioner.

PUZZOLANIC CEMENT (TRASS) TESTS

The natural zeolites are potential cementadditives due to their SiO2 and Al2O3 contents.They have puzzolanic features which can bedefined as, because of their high SiO2 and Al2O3contents, they can form binding products whenreacted with dead lime (Ca(OH)2) and water. So,they can be used as puzzolans in cements andconcrete systems. Addition of puzzolans tocements and concrete systems increase thepermeability and workability of the concrete andsimilarly increase the resistance to external fac-tors such as alkali silica reaction and sulphateeffect (Uzal et al., 2003).

In puzzolanic activity tests, crushed tras (thisis a silica and alumino-silica bearing tuff, a natu-ral puzzolanic material, and it does not have anyhydrolic property when it is used alone, butwhen crushed in to small particles, in aquaeousmediums and with calcium hydroxide under nor-mal temperature, it starts chemical reaactionsand displays hydraulic properties), dead limemixture and standard sand is used.

The tests for it to be used as cement-additivematerials are conducted according to “TS 25 –April 1975 Trass” standard. For it to be used ascement additive, the preliminary conditions areas follows:

Total % SiO2+Al2O3+Fe2O3 must be higher than 70%,

% MgO must be 5.0 % maximum,

% SO3 must be 3.0 % maximum, and,

% A.Z. must be 5.0 % maximum.


Table 10- Results of flexural and compressive strength tests of the samples.

Puzzolanic activity of the samples were cal-culated according to “TS 25 April 1975” stan-dard. According to TS 25 the flexural strengthand compressive strength must be at least 10kgf/cm2 and 40 kgf/cm2, respectively.

The tests to evaluate zeolite as cement addi-tive material were started acccording to the suit-ability of the results of the density and chemical

analyses. According to the standard (TS 25), therequested minimum 7 days compressionalstrength must be 40 kgf/cm2, and 7 days flexur-al strength must be at least 10 kgf/cm2.

Accordingly, when the table 10 is studied, wesee that the samples FO-35 and B-2 can beused as cement additive materials.

RESULTS AND DISCUSSIONS

Technological and mineralogical researchwas conducted to determine the areas of usageof the zeolites collected from İzmir-Foça,Balıkesir-Bigadiç and Manisa-Gördes regions.

The minerals determined after thin sectionstudies and XRD analyses and the results ofXRF analyses of the samples collected from thestudy areas were given as tables.

In this study which aims to determine theareas of usage of zeolite, research was conduct-ed to see whether they can be used in ceramic,

paper industries and as cat litter and cementadditives. Some samples were found to be suit-able to be used in ceramic, paper and cementindustries.

As a result of the mineralogical and techno-logical analyses the samples FO-35 and B-2were found suitable to be used as cement addi-tives. The sample B-6 ca be used as soil condi-tioner according to the regulations published inthe Official Gazzette dated 04.05.2004 andnumbered 25452. It was shown that the samplesFO-20, FO-35 and KIR-3 displayed whitenessvalues which indicate they can be used as fillingmaterials in paper industry, however, since this


sample has high abrasion index, its percentageamount must be decreased depending on thetype of the paper being produced.

Manuscript received May, 14, 2008

REFERENCES

Albayrak, M., 2008. Batı Anadolu, Trakya,Kapadokya Yöresi Zeolitleri MineralojikVeri , (unpublished).

Albayrak, M., Karahan, S. and Atlıhan. S., 2001.“Zeolitten Hafif Yapı Gereci Üretilme-si(Zeoton 2000)”, MTA Servisi, DerlemeRapor No: 10471. Ankara, (unpub-lished).

Ataman, G., 1977. Batı Anadolu Zeolit Oluşum-ları,Yerbilimleri Dergisi, H.Ü Yayını 3, 85

Ercan, T., 1983. Gördes Volkanitlerinin (Manisa)Petrolojisi ve Kökensel Yorumu, TürkiyeJeoloji Kurultayı Bülteni, 26. 41-49.

______, Türkecan A., Günay E., Çevikbaş A.,Ateş M., Can B. and Erkan M., 1984a.Dikili Çandarlı Bergama (İzmir) ve Ay-valık Edremit Korucu (Balıkesir) Yörele-rinin Jeolojisi ve Mağmatik KayaçlarınPetrolojisi. MTA Genel Müdürlüğü Der-leme Rapor No: 7600, Ankara, (unpub-lished).

Ercan, T., Güney, E., Çevikbaş, A., Ateş, M., Kü-çükayman, A., Can, B., Erkan, M.,

1984b. Bigadiç Çevresinin (Balıkesir) Je-olojisi, Magmatik Kayaçların Petrolojisive Kökensel Yorumu, MTA Derleme Ra-por No: 7601, Ankara, (unpublished).

Esenli F., 2002. Türkiye’de Doğal Zeolit Rezerv-leri, Madenciliği, Üretim ve Pazar

Durumu,Zeolit Sempozyumu, TÜBİTAK-MAM,24 Haziran 2002, Gebze, Kocaeli,1-10.

Göktaş,F., 1996. Gördes Neojen Havzasının Je-olojisi,MTA Derleme Rapor No: 9931,Ankara, (unpublished).

Kalafatoğlu, İ.E., 2002. Zeolit Araştırmaları Tür-kiye Bibliyografyası, Tübitak MAM, Malzeme ve Kimya Teknolojileri Araştır-ma Enstitüsü.

Lengeranlı,Y., Baykal,A., Sun,A., Işın, R., Met-li,F., Avşar,M., Türkbileği,H., Tan,T. andKurt, H.İ., 1998. İzmir İlinin Çevre Jeolo-jisi ve Doğal Kaynakları Raporu.No:10137, İzmir.

Öner, F., Albayrak, M. and Kayabalı, İ., 2000.“Zeolitli Tüflerin Jeolojik, Mineralojik,Kimyasal özellikleri ve Sanayide Kulla-nılabilirliğinin Araştırılması”, MTA Derle-me Servisi, Rapor No. 10338, Ankara(unpublished).

Resmi Gazete, 2004. “Tarımda Kullanılan Orga-nik, Organomineral, Özel Mikrobiyal veEnzim İçerikli Organik Gübreler ile Top-rak Düzenleyicilerin Üretimi, İthalat, İh-racat, Piyasaya Arz ve Denetimi” Yönet-meliği, sayı no:25452 .

Türk Standartları Enstitüsü., 1975. TS 25- Nisan1975 Tras

______, 1987. TS 699 -Ocak 1987 Tabii YapıTaşları Muayene ve Deney Metotları

______, 1997. TS 2583 EN ISO 787- 5 - Aralık1997 Pigmentler ve Türk StandartlarıEnstitüsü., Dolgu Maddeleri İçin GenelDeney metotları-Bölüm 5:Yağ Absorpla-ma Değerinin Tayini

______, 1992. TS 10521- Aralık 1992 Talk - Ka-ğıt Sanayinde Kullanılan

Türk Standartları Enstitüsü, 1995. TS 11653-Ni-san 1995 Kalsit - Kağıt Sanayinde Kul-lanılan

______, 1997. TS 12131- Şubat 1997 Sepiyolit -Kedi Kumu Üretiminde Kullanılan

______, 1987. TS 5396- Aralık 1987 Kaolin-Se-ramik Sanayinde Kullanılan

Uzal B., Bektaş F. and Turanlı L. 2003. “Öğütül-müş Doğal Zeolitin Alkali ve Sülfat Etki-si ile Genleşmesinin İncelenmesi. 5.Ulusal Beton Kongresi / İstanbul, Bildiri-ler, 403-409.

Vural A. and Albayrak M., 2005 Gördes ve Civa-rı Zeolitlerinin Mineralojisi. 58.Türkiye Jeoloji Kurultayı Bildiri Özleri, 11-17 Ni-san, MTA Kültür Sitesi, Ankara

Yağmurlu, F., 1983. Akhisar Doğusu, NeojenTopluluğu’nun Jeolojisi ve Kömüryatakları ile olan ilişkisi. Dokuz EylülÜniversitesi Fen Bilimleri Enstitüsü,Doktora Tezi. 217 s. İzmir

______, 1983. Akhisar Doğusu, Neojen Tortulla-rın Depolanma Ortamları ve Kömür ya-takları ile olan ilişkisi. Türkiye Jeoloji Ku-rultayı Bildiri Özetleri.

Yücel H., 1987. “Zeolitler ve Uygulama Alanları“III. Ulusal Kil Sempozyumu, Bildiriler,s391-402.

sedimentological- stratigraphical evaluation of …

Documents