ARTICLE IN PRESS

Quaternary International 199 (2009) 157–163

Forum Communication Development of the Cambazlı (Turgutlu/) fissure-ridge-type travertine and relationship with active tectonics, Gediz Graben,

H. Haluk Selima,Ã,Gu¨rsel Yanikb

aDepartment of Geology Engineering, Kocaeli University, Kocaeli 41040, Turkey bDepartment of Geology Engineering, Dumlupınar University, Ku¨tahya, Turkey Available online 28 May 2008

Abstract

Travertine occurrences in the Cambazlı village area exist at the western edge of the Gediz Graben, comprising the Turgutlu Neogene basin. The ‘‘Cambazli travertine’’ was classified into two main groups based on physical, mineralogical and petrographic properties. Occurrences of travertine are probably due to faulting between the Paleozoic units of Menderes Massif and the Pliocene Kanlıtepe Formation. Group I travertine is horizontal and oriented NE-SW and NW-SE, whereas Group II travertine occurrences are oriented E-W direction. The Cambazlı travertine is a fissure-ridge type. Travertine continues to develop both in fissures and on the topographic surface as bedded deposits. Layered travertine is deposited on both surfaces of fissures. It develops either symmetrically or asymmetrically with respect to the centre of the fissure. Kinematical analyses of listric normal fault measurements demonstrate that NNE-SSW extension occurred. The Cambazlı travertine in the Gediz Graben has been deposited by hydrothermal waters rising through fracture systems, probably related to an active listric normal fault developed in the north of the study area. r 2008 Elsevier Ltd and INQUA. All rights reserved.

Keywords: Extensional tectonics; Fissure-ridge type travertines; Gediz Graben system; Active tectonics

1. Introduction and also between faulting, a major mechanism for the transfer of hot water into to the surface. Fissure-ridge Hancock et al. (1999) discussed the use of travertine travertine occurs as water flow in both sides of fissures. deposits as indicators of active tectonics. Their study was Fissure-ridge-type travertine formations are deposited by based on observations in several Mediterranean areas, Na-bicarbonate waters rising through fissures and flowing including some of most well-known deposits, such as to the topographic surface around this fissure. As a result, Pamukkale in Turkey. Grabens of western , a ridge is formed by the accretion of Na-bicarbonate together with several Mediterranean areas are extremely deposits along the fissure (Fig. 2). rich in travertine deposits. The Cambazlı travertine is part of the Gediz Graben system (Fig. 1). In western Anatolia, travertine occurrences formed in the active fault zones have 2. Geological setting been observed by many researchers (Altunel, 1994; C- akir, 1996). Wyatt (1986) emphasized that travertine is generally 2.1. Stratigraphy deposited around springs. Altunel (1994) and Altunel and Hancock (1993, 1996) examined the joints developed in In the study area, the basement is formed of the travertine of the Pamukkale (Denizli) area. Sibson et al. Paleozoic Menderes Massif, mica schist, phyllite, meta- (1975) and Barnes et al. (1978) indicated a close relation- sandstone and crystallized limestone. Gray crystalline ship between travertine occurrences and tectonic activity, limestone at the base grades to white dolomite at the top. Ophiolitic rocks of the I˙zmir-Ankara Zone overlie marbles ÃCorresponding author. Tel.: +90 262335 1148; fax: +90 26 2335 2812. of the Menderes Massif rocks along a low-angle thrust E-mail addresses: [email protected] (H. Haluk Selim), fault. The ophiolitic complex, including serpentines, [email protected] (G. Yanik). extends towards the west and north-west. The Kanlıtepe

1040-6182/$ - see front matter r 2008 Elsevier Ltd and INQUA. All rights reserved. doi:10.1016/j.quaint.2008.04.009 ARTICLE IN PRESS 158 H. Haluk Selim, G. Yanik / Quaternary International 199 (2009) 157–163

Fig. 1. Location map of Cambazlı travertine, grabens and fault system of the western Anatolia (view of the Landsat 7).

Fig. 3. Stratigraphy of the study area (Yanık, 2005).

level. The most prominent elements of the geomorphology Fig. 2. A model of deposition of fissure-ridge-type travertine occurrences in the region are uplifted and depressed areas bounded by (Altunel and Hancock, 1998). normal faults. The youngest units in the region are located in the lowest area while the oldest units are located in the ¨ formation consists of Pliocene sediments (Unay et al., highest area. In addition, antithetic faults trending NW–SE 1995; Emre, 1996; Yusufog˘lu, 1996). The Quaternary in the basin are intersected by normal faults (Fig. 6). The alluvium and travertine are the youngest units at this study area was initially raised along the low-angle normal margin (Fig. 3). Travertine occurrences have been classified faults, but later the margin was elevated by the high-angle into two different units (Groups I and II) based on normal faults which cut and displace the low-angle faults field observations and mineralogical–petrographic studies (Yanık and Selim, 2004; Yanık, 2005)(Fig. 7). The (Figs. 4 and 5). Travertine in the region developed above northern margin of the Gediz Graben is morphologically the faults between the Paleozoic Menderes Massif rocks less marked and has seismically inactive high-angle normal and the Pliocene Kanlıtepe formation. Group I travertine faults (So¨zbilir, 2002). oriented NE–SW and NW–SE and is horizontal. Group II Travertine covers an area of 5 km2 at present. Tempera- travertine is oriented E–W (Yanık, 2005). ture of the hot waters varies from 34 to 85 1C and pH values vary between 6 and 8. Travertine occurrences are 2.2. Tectonic setting products of the faulting between the Paleozoic Menderes Massif and the Pliocene Kanlıtepe Formation. The The topography is asymmetric, being steeper along the Cambazlı travertine, located 10 km NE of Turgutlu, northern side of graben where Mount C- aldag˘rises to over generally consists of layers with 50–200 m length and 1000 m from the present-day graben base, 100 m above sea 10–60 cm thickness. The southern outcrop of the lower ARTICLE IN PRESS H. Haluk Selim, G. Yanik / Quaternary International 199 (2009) 157–163 159

Fig. 4. E–W trending Group II travertine photographs (a and b). level is steep-sided and collapsed in some places along the Gediz River. Travertines have irregular and various size pores from mm to cm scale. Some macropores and fractures were filled by seepage of white marl at the top. In microscopic scale, small pores are partially or com- pletely filled with light-coloured calcite spar. Hot waters emerging from fissures and saturated with sodium bicarbonate and minerals deposit orange, brown and cream colored travertine in the walls of fissures. On the walls of the fissures, parallel to the fissures, compact thin layered and hard laminated travertine crusts have been deposited. The Cambazlı travertine has been assigned to two groups, band thickness and erosion rate. Group I consists of eight fissure-ridge travertines exposed in the study district, with a band thickness ranging from 10 to 60 cm (Fig. 8). The Group II travertine occurrences are light beige-white, whereas thin banded older (Group I) traver- tine is light beige-yellowish. The massive Group II travertine has highly porous mosaic lenticular textures. Fig. 5. The Group I-layered travertine occurrence and fissure (a–c). Group II travertine contains Fe-oxide minerals and plant remnants. Physical and mechanical test results for this ARTICLE IN PRESS 160 H. Haluk Selim, G. Yanik / Quaternary International 199 (2009) 157–163

Fig. 6. Geological map of study area.

Fig. 8. Morpho-tectonic map of fissure-ridge-type Cambazlı travertine.

Table 1 Properties of the Groups I and II travertine

Properties Group I travertine Group II travertine

CaCO3 (%) 96.7 97.4 MgCO3 (%) 2.6 2.2 SiO2 (%) 0.04 0.05 Insoluble material (%) 0.6 0.4 Specific gravity (gr/cm3) 2.7 2.4 Fig. 7. The cross-section of Cambazlı travertine and listric normal faults. Water absorption (%) 1.0 2.0 Porosity (%) 2.5 3.0 Compressive strength (N/mm2)60 3 travertine are shown in Table 1. The Group II travertine Index of whiteness (%) 75 83–90 has an 83–90% index of whiteness. Physical and mechanical tests such as specific gravity, water absorption, porosity and compressive strength values 3. Discussion for the Group I travertine were 2.7 gr/cm3, 1%, 2.5% and 60 N/mm2, respectively. For the younger (Group II) Western Turkey comprises several continental fragments travertine, the corresponding values are 2.4 gr/cm3, 2.0%, with distinctive stratigraphic, structural and metamorphic 3.0% and 3 N/mm2. The Cambazlı travertine occurrences features that were amalgamated by continent–continent also provide information about the direction and rate of collision during Alpine orogeny and the following con- recent crustal extension in the Gediz Graben. Banded sumption of the intervening Neo-Tethyan oceanic litho- travertines are formed by precipitation from rising hot sphere by northward-dipping subduction (S-engo¨rand water on the fracture walls. The precipitation develops Yılmaz, 1981; Okay, 1989). West Anatolia lies within a progressively from the outer wall to the center of the region of rapid continental crustal extension (S-engo¨r et al., fracture during the opening of the fracture related to the 1985; Bozkurt, 2000) and is a counterpart of the Aegean regional extension. Sea in the eastern Mediterranean (Westaway, 1990). ARTICLE IN PRESS H. Haluk Selim, G. Yanik / Quaternary International 199 (2009) 157–163 161

Different mechanisms have been proposed for the origin of extensional tectonics in the Aegean horst-graben system. The Gediz Graben is a part of basin and range style graben system in the western Anatolia. The Gediz Graben (also known as the Alas-ehir Graben) is an arc-shaped structure trending NW–SE between Alas-ehir and , but trending E–W and ENE–WSW between Salihli and Turgutlu. It is one of the main extensional structures in west Turkey with a length of 140 km and a width of 15 km, which increases in the western part where the graben merges with the Soma––Manisa basin. Small NW–SE trending basins form the Mount C- aldag˘sector. The south side of the Gediz Graben is bounded by a major fault (the main southern boundary faults) separating the Neogene sediments of the graben from the metamorphic basement (Menderes Massif). Further to north in the Fig. 9. Asymmetric view of Cambazlı travertine (Group I). graben a sub-parallel fault separates Neogene and Qua- ternary sediments (U¨rgu¨n, 1966; Yag˘murlu, 1987; Dora et al., 1992; Emre, 1996, 1998; Ediger et al., 1996; Gu¨rsoy et al., 1997; Tarcan and Filiz, 1997; Yılmaz, 1997; Hakyemez et al., 1999; Koc-yig˘it et al., 1999; Bozkurt, 2000; Yılmaz et al., 2000; So¨zbilir, 2001 and 2002; Yanık, 2005). The age of the graben is considered to be Miocene–Pliocene, but no specific data are available (Seyitog˘lu and Scott, 1996). Travertine develops as banded deposits in fissures and as layered deposits on the topographic surface. Layered travertine deposited on the ground surface is inclined away from the fissure. Dips of bedding vary from a few degrees to as much as 801 and roof-like travertine can be symmetric or asymmetric with respect to the center of fissure (Fig. 9) Fig. 10. Seismic-section of a listric normal fault (from Werncke and due to topographic irregularities. Travertine ridges vary Burchfiel, 1982). from a few meters to 200 m in length, from 1 to 5 m in

Fig. 11. Kinematical analyses of listric normal fault measurements taken from Neogene units by stereogram show that extension occurred along NNE–SSW direction. ARTICLE IN PRESS 162 H. Haluk Selim, G. Yanik / Quaternary International 199 (2009) 157–163 width, and from 50 cm to 15 m in height. In the light 4. Conclusions of the present data, Cambazlı travertine in the Gediz Graben is deposited by hydrothermal waters rising The aim of this study was to explain travertine through fracture systems probably related to an active occurrences in relation to the extensional settings, espe- listric normal fault developed in the north of the study cially in the Gediz Graben extensional province. The area (Fig. 10). Menderes Massif and I˙zmir-Ankara Zone on the approxi- The main mechanism responsible for the formation of mately east–west direction comprise two uplifts and there is Cambazlı travertine is linked to the conditions proposed a depression area between these uplifts in the study area. for the graben system (Werncke and Burchfiel, 1982; Young sediments in the depression area consist of Neogene Altunel and Hancock, 1993, 1996, 1998). In western and Quaternary sediments. E–W-oriented high-angle nor- Anatolia, approximately E–W trending grabens and their mal faults have been cut off by antithetic faults oriented basin-bounding active normal faults are the prominent N–S. The east–west extended basin is bounded by nearly neotectonic features. The Gediz Graben system is one of east–west normal faults developed as a result of the these features formed by E–W, NW–SE and NE–SW extensional tectonic regimes in western Anatolia. The trending normal faults associated with antithetic and normal faults bounding the north and south part of the synthetic secondary faults (Yanık and Selim, 2004). The study area form the Gediz Graben system and cause seismic activity of the Gediz Graben can be defined by seismic activities in the region. In the Gediz Graben, recorded earthquakes, such as the 2 March 1965 Salihli Cambazlı travertine is deposited by hydrothermal waters (M ¼ 5, 8), 28 March 1969 Alas-ehir (M ¼ 6, 5) and 28 rising through fracture systems probably related to an March 1970 Gediz (M ¼ 7, 2) earthquakes (Ergin et al., active listric normal fault, developed in the north of the 1967; Eyidog˘an, 1988; Eyidog˘an et al., 1991). The region is study area. On the walls of the fissures, parallel to the under the influence of an active extension regime today. fissures, compact thin layered and hard laminated traver- These earthquakes caused damage along Gediz Graben tine crusts were deposited. located in residential areas. Several travertine deposits are Two travertine units were defined in the study area based present in Gediz and Alas-ehir (Eyidog˘an et al., 1991). In on their differences and mineralogical and petrographic addition, there are several hot springs, spa and travertine properties. It is suggested that the Group II travertine is deposits located along the normal faults bordering the relatively younger than Group I. Kinematical analyses of northern edge of the graben. In the study area, layered normal fault measurements taken from Neogene units by travertine occurrences formed by the NNE–SSW trending stereogram show that extension occurred approximately extensional tectonics graben which controlled by normal NNE–SSW, compatible with Group II travertine fissure faults developed the Cambazli fissure-ridge-type travertine. strikes. The Cambazlı travertine where the hot springs are Hot springs were observed along the E–W trending Group still active forms as ‘‘fissure-ridge type’’. The Pamukkale II travertine-generated active faults in the Gediz Graben travertine occurred due to an extensional tectonic regime. system. Axes directions of Group II travertine fissures are The Pamukkale area and the Gediz Graben are not similar compatible with the active tectonics in the region and in terms of tectonic activity; however, travertines in both related to the regional active tectonic regimes. Kinematical basins morphologically resemble each other. analyses of listric normal fault measurements taken from Neogene units by stereogram show that extension occurred References approximately NNE–SSW, which is compatible with Group II travertine fissure strikes (Fig. 11). Similar studies Altunel, E., 1994. Active Tectonics and Evolution of Quaternary by Zanchi and Angelier (1993) and Kıratzi and Louvari Travertines at Pamukkale, Western Turkey. Ph.D. Thesis, University (2003) indicated that focal mechanism solutions of the of Bristol, unpublished. recent earthquakes yielded identical results with the Altunel, E., Hancock, P.L., 1993. Morphological features and tectonic general trend of extensional-type features. Group II setting of Quaternary travertines at Pamukkale plateau, western Turkey. Geological Journal 28, 335–346. travertine fissures strike approximately E–W while Group Altunel, E., Hancock, P.L., 1996. 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