Open Geosci. 2015; 7:446–464

Research Article Open Access

Murat Gül* Occurrences of Chert in Jurassic-Cretaceous Calciturbidites (SW Turkey)

DOI 10.1515/geo-2015-0029 ubility controls silica precipitation, it increases with tem- perature and pH values (especially pH>9) [2]. Received November 25, 2013; accepted February 20, 2015 Chert can be deposited via organic and inorganic path- Abstract: The Lycian Nappes, containing ophiolite and ways [3]. Silica-secreting organisms play an important sedimentary rocks sequences, crop out in the southwest role in organic chert deposition and silica precipitation, Turkey. The Tavas Nappe is a part of the Lycian Nappes. in water undersaturated with silica [2]. These organisms It includes the Lower Jurassic-Upper Cretaceous calcitur- are the radiolarians, diatoms, silicoagellates and opa- bidites. Chert occurrences were observed in the lower part line silica-shelled microplankton [2]. Many studies have of this calciturbidite. These cherts can be classied on the focused on these organisms, especially on the radiolar- basis of length, internal structure and host rock. Chert ians [4–6]. The inorganic chert formation requires over- bands are 3.20-35.0 m in length and 7.0-35.0 cm thick. Chert saturated solutions with silica and silica replacement [3]. lenses are 5.0-175.0 cm in length and 1.0-33.0 cm thick. Ac- The silica may be sourced from rivers, mid-ocean ridge vol- cording to its internal structure, granular chert (bladed- canic products that reacted with sea water, and silica par- large equitant quartz minerals replaced the big calcite ticles on the sea oor [2]. The enrichment of silica is also mineral of fossil shell) and porcelanious chert (microcrys- related to diagenetic eects and replacement of older min- talline silica replaced micrite) have been separated. Cherts erals [2, 3, 7–11]. Chert formation-chertication during di- are generally associated with calcarenite-calcirudite, the agenesis aects the porosity, strength and density of the others with calcilutite. Micritic calcite patches of cherts rocks, and these in turn control reservoir characteristics point out an uncompleted silicication. The source of sil- [3, 8, 12]. ica was dominantly quartz-rich, older, basal rocks and to Most of the chert was found in the key stratigraphic a lesser extent radiolarians. The coarse-grained calcitur- level or in the structurally allochthonous packages [13]. bidites act as a way for silica transportation. Some calcite Cherts form in small nodules, lenses or thin discontinu- veins (formed during transportation and emplacement of ous and continuous beds [1, 2, 7]. Relict structures of chert nappes) cut both calciturbidites and cherts. Thus, chert oc- nodules inside limestone point out the replacement dur- currences evolved before emplacement of nappes (the lat- ing diagenesis [2, 3]. Therefore, studies on chert formation est Cretaceous-Late Miocene period) during the epigenetic provide data about the general geological and paleogeo- phase. graphic evolution [3, 5–7, 13–15]. Keywords: Chert band; Chert lens; Radiolaria; Calcitur- Chert developments, found in various aged limestones bidite; silicication crop out in the dierent part of world [10]. Detailed sed- imentological and geochemical aimed studies of cherts have determined that they may have been deposited under dierent environmental conditions [2, 3, 5–8, 10, 13–15]. 1 Introduction The examined cherts are situated in structural unit called the Lycian Nappes (Figures 1 and 2) [16–19]. The Lycian Chert is a dense, extremely hard, microcrystalline and Nappes contain ophiolite and sedimentary rock bearing cryptocrystalline quartz bearing siliceous sedimentary nappes [16–19]. Each nappe has been called dierent rock [1]. The silica ratio and environmental conditions are names [16–19]. One is the Tavas Nappe, which contains the main controlling factors of silicication. The silica sol- calciturbitides. These calciturbidites contain calcilutite, calcarenite and calcirudite, and a great number of chert occurrences in lower part [16, 19]. The Paleozoic quartz bearing detrital rocks were seen at the bottom of chert lev-

*Corresponding Author: Murat Gül: Mugla Sıtkı Kocman Univer- els, while basic volcanic and clastics located at the top of sity, Engineering Faculty, Department of Geological Engineering, chert levels (Figure 3) [16, 19]. 48000, Kotekli, Mugla, Turkey, E-mail: [email protected] © 2015 M. Gül, licensee De Gruyter Open. This work is licensed under the Creative Commons Attribution-NonCommercial-NoDerivs 3.0 License. The article is published with open access at www.degruyter.com. Occurrences of Chert in Jurassic-Cretaceous Calciturbidites (SW Turkey) Ë 447

Cherts of the Tavas Nappe form bands and lenses of Jurassic bioclastic limestone, Middle Jurassic-Upper Creta- various lengths and widths. Their internal structures and ceous carbonate debris-ow deposits, turbidites and mi- lower-upper surface characteristic are also variable. The crite and lithic turbidites in its upper part. calcite mineral structure of calciturbidites had a certain ef- S˛enel (1997, 2007) separated the C˛enger Formation fect on chert internal structure. Another important issue: at the bottom of Tavas Nappe. It contains Triassic-Lower the silicication was not complete, even in chert bodies. Jurassic sandstone, conglomerate and mudstone (0.2-350 The aim of this study is to investigate the sedimentological m thick; uvial-alluvial fan, back shore at the top). Then, and petrographic characteristics of chert to determine the the Liassic Ağac˛lı Formation (products of shallow sta- controlling factors of silicication and types of chert based ble carbonate shelf) consists of 450 m thick algae and on eld observations and detailed petrographic analysis. coral bearing limestone and dolomitic limestone [16]. The Babadağ Formation (650-1020 m) starts with Toarcian red- colored Ammonitica Rosso bearing limestone that uncon- 1.1 Geological background formably overlies the Ağac˛lı Formation. Then, it contin- ues with Dogger-Maastrichtian cherty micrite, radiolarite, The southwest Turkey contains the Menderes Metamor- chert and shale. In some areas, the Babadağ Formation in- phic Massif, the Lycian Nappes, and the Beydağları Au- cludes Lower Cretaceous cherty micrites (examined in this tochthon from north to south (Figure 1) [16–23]. The Ly- study), radiolarite, chert, shale, and then calcarenite and cian Nappes consist of many nappe slices. They have been calcirudite. The Globotruncana sp. bearing micrites and separated by faults and called by dierent names (Fig- rudist bearing calciturbidites are located at the top. The ure 2) [16–19, 21]. The examined cherty limestone is a part Babadağ Formation was interpreted as a product of conti- of the Tavas Nappe, which is surrounded by the Bodrum nental slope and basin margin [16, 19]. It is unconformably Nappe (Figure 2) [16, 19]. These two nappes were also ex- overlain by Upper Paleocene-Lutetian Ölüdeniz volcanics amined under the name of Köyceğiz Thrust Slabs [17, 18]. (including basalt and red colored micrites) and the Faralya The ophiolitic mélange and peridotite slabs tectonically Formation (cherty micrite, clayey limestone, calcarenites- overlie them [16–19, 21]. calciturbidites, basic volcanics; Figure 3) [16, 19]. The Tavas Nappe unconformably overlies the Paleo- The Tavas Nappe is surrounded by the Bodrum zoic Karadağ and Tekedere Series [16, 19]. The Karadağ Nappe-C˛ökek Units. These units consist of Upper Triassic- Series contains Upper Paleozoic quartzite, shale, shale- Jurassic dolomites (the Kayaköy Dolomite), limestone limestone alternations, and dolomitic limestone that are and dolomitic limestones (the Sandak Formation), Up- unconformably overlain by Triassic quartzite, limestone, per Jurassic-Cretaceous calciturbidite and cherty biomi- and sandstone-shale. The Tekedere Series consists of crites (the Göc˛gediği Formation), and Upper Senonian Lower Carboniferous volcanic rocks, chert, limestone, sandstone, conglomerate, claystone and limestone (the sandstone-siltstone-claystone, Upper Permian limestone Karaböğürtlen Formation; Figures 2 and 3) [16, 19]. and dolomite (Figure 2). However, Collins and Robertson (1998, 1999) reported that the Karadağ Series is composed of Upper Paleo- 2 Methods zoic limestone, Lower Triassic quartz arenite and lime- stone, Upper Triassic limestone, lithicarenite and shale. It is tectonically overlain by the Teke Dere Thrust Sheet. Cherty levels of the Bozburun Hill I Section (30 m; Fig- Collins and Robertson (1998, 1999) described the con- ure 4) and Bozburun Hill II Section (15 m; Figure 5; ini- tents of the Teke Dere Thrust Sheet broadly than S˛enel tially presented in Gül et al., 2013) were analyzed in detail. (1997, 2007). The Teke Dere Thrust Sheet contains Per- These two sections are separated by normal faults [22]. The mian basalt, radiolarite and limestone in its lower part; basements of sections consist of cherty calcilutite alter- unconformably Triassic sandstones, Lower-Middle Juras- nated with calcarenite, and calcirudite (Figures 3, 4 and 5). sic bioclastic limestones, Upper Jurassic-Upper Cretaceous The Bozburun Hill I Section includes more calciturbidite pelagic micrite and distal calciturbidite in the middle; and in its upper part. The length and thickness of cherts were Upper Paleocene-Eocene basalt, radiolarite and debris measured in detail. Cherts have been classied as a band ow deposit in its upper part. It is tectonically overlain by (length > 3m) and lens (Table 1). The dimensions of chert the Köyceğiz Thrust Sheet. It consists of Middle-Upper Tri- bands and lenses have been evaluated statistically for both assic mid-ocean ridge volcanic, volcanoclastic turbidites sections (Tables 2 and 3). The irregularities of upper and in its lower part; Upper Triassic pelagic biomicrites, Lower lower surface of chert have been noted for detail classica- 448 Ë M. Gül

Figure 1: The distribution of important geologic units of the Southwest Turkey [20]. The Lycian Nappes was developed in the northern side of the Menderes Metamorphic Massive, and then it was transported and emplaced to the south.

Figure 2: The distribution of dierent segments of the Lycian Nappes in and around the study area (modied from Şenel, 1997). The con- tacts between nappes are generally tectonic. Occurrences of Chert in Jurassic-Cretaceous Calciturbidites (SW Turkey) Ë 449

Figure 3: The detailed geologic map of study area (modied from S˛enel, 1997).

Table 1: Chert types determined in calciturbidites based on length.

Chert Types Band (L>3 m) Smooth lower and upper surface Wavy lower and upper surface Lens (L<3m) Single Irregular lower and upper surface Regular lower and upper surface Multiple Irregularly combined – elongated Regularly combined - elongated

Table 2: Statistical evaluation of Chert Bands Measurements.

Chert Band Bozburun I Bozburun II All sections Length (cm) Thickness (cm) Length (cm) Thickness (cm) Length (cm) Thickness (cm) Measurements (N) 2 5 7 Maximum (cm) 600 35 3500 30 3500 35 Minimum (cm) 400 27 320 7 320 7 Average (cm) 500 31 1794 21.6 1424.3 24.3 Standart Deviation 141.4 5.7 1211.7 8.8 1175.1 8.8 450 Ë M. Gül

Figure 4: The Bozburun Hill I Measured Section [22]. Occurrences of Chert in Jurassic-Cretaceous Calciturbidites (SW Turkey) Ë 451

Table 3: Statistical evaluation of Chert Lens Measurements.

Chert Lens Bozburun I Bozburun II All sections Length (cm) Thickness (cm) Length (cm) Thickness (cm) Length (cm) Thickness (cm) Measurements (N) 15 35 50 Maximum (cm) 150 33 175 28 175 33 Minimum (cm) 16 4 5 1 5 1 Average (cm) 62.9 11.9 50.1 9.7 53.9 10.4 Standart Deviation 44.4 8.2 43.3 5.5 43.6 6.4 tion. Internal structure of cherts has been classied in two groups: big quartz bearing granular and microcrystalline- cryptocrystalline (?) quartz bearing porcelanious chert. The host rocks of chert have been dened as calcilutite, and calcarenite-calcirudite (Figures 6 and 7). The petro- graphical classications of thin sections were made ac- cording to dierent researchers [24–26]. Seven chert sam- ples were collected for petrographic analysis (Table 4; Fig- ure 8). The petrography samples were selected from dier- ent types of cherts (Table 4).

3 Results

After the base level, 4.5 - 5 meter section of the Bozburun Hill I Section contains abundant micritic limestone (calci- lutite) and rarely calcarenites (Figures 4 and 6). The ini- tial three levels of this part include cherty levels. The B12 sample was taken from micritic limestone-calcilutite level located at the base of rst chert band (Table 4; Figure 4). Then, 6 m long and maximum 35 cm thick chert band was found. It comprises two parts; a cream-colored lower part shows a granular appearance (B11 chbl (chert band lower part) sample; Table 4; Figures 4, 6B, 8G and 8H), and hard, cream-gray colored upper part shows a porcelanious view (B11chbu (chert band upper part) sample; Figures 4, 6B). Later 2 m of the section contains alternating calcarenite and micritic limestone-calcilutite, (B13 and B10 samples; Table 4; Figures 4, 6B, 8I and 8J) with chert lenses (B14 chl (chert lens) sample; Figure 8K). Then, 3 m thick cal- carenite and calcilutite alternations are situated (B8 sam- ple; Figures 8E and 8F). This section also consists of a great number of chert lenses, (B7 chl sample; Figures 4, 8A and 8B) and to a lesser extent, chert bands (B9 chb sample). The rest of this section is composed of calcirudite and cal- carenites with varying thickness and smaller amounts of calcilutite levels (Figsures 4 and 6). Figure 5: The Bozburun Hill II Measured Section (explanations are given in Figure 4) [22]. 452 Ë M. Gül

Both lower and upper parts of the Bozburun Hill II ments were performed on the Bozburun Hill II Section. The Section have been cut by faults (Figures 5 and 7). Beige- length of Bozburun Hill I Section single lenses varies be- colored micritic limestone-calcilutite (8.5 m thick; sample tween 16.0 and 150.0 cm, while thicknesses range between B15) levels are located at the bottom part of this section. 4.0 and 33.0 cm. The length of Bozburun Hill II Section sin- The numbers of chert band and chert lens (B16chl sample; gle lenses vary between 28.0 and 175.0 cm, with thickness Figure 8L) in this section are higher than the Bozburun Hill ranges between 1.0 and 28.0 cm (Table 3). The calcarenites- I Section. The color of cherts in this section is usually milky calcirudites are situated either above or below the majority brown. Two layered chert band (lower granular and up- of the lenses. per porcelanious) are located in this part. Calcilutite also The single chert lenses generally have smooth lower comprises chert lled thin vessels (Figure 7B). Chert lens, and bottom surfaces (Figures 6E and 7B). However, as in case of the Bozburun Hill I Section, formed single or calcarenite-calcirudite at the top of chert lenses cause ir- combined lens (including two or more lenses). This section regular upper surface development (Figure 6F). contains calcirudite and calcarenite levels in its upper part The multiple lenses are classied as regularly elon- that includes chert lenses only in its rst meter (Figures 5 gated or irregularly elongated multiple lenses (Table 1). and 7). The regularly elongated multiple lenses contain two or The cherts of Bozburun Hill Sections have been clas- more lenses laterally at the same level (Figures 6C, 6D, 7B sied based on their length, internal structure and host and 7C). They are similar to bands, but are shorter. This rocks. The microscopic features of chert can supply infor- type is generally found in the Bozburun Hill II Section. The mation about diagenetic properties. irregularly elongated multiple lenses contain two or more lenses; however they are not found laterally at the same level (Figure 6C). This type is seen widely in the Bozburun Hill I Section. The calcarenite-calcirudite levels led to de- 3.1 Chert types based on length velopment of multiple lenses with dierent thickness, and they also intrude to the multiple lenses (Figure 6C). These The classication of chert of the Babadağ Formation based intrusions led to distortion and deformation of integrated on length is presented in Table 1. In this study, cherts that lenses. The small scale synsedimentary fault also led to de- have 3 m or longer lateral continuity are classied as chert velopment of the irregularly elongated multiple lenses. band. Cherts that have a lateral continuity shorter than 3 m are classied as a chert lens. Chert bands, especially in the Bozburun Hill II Sec- tion, have a smooth bottom and upper surface (Figure 7A). The rest of chert bands have wavy surfaces (Figure 6B). All 3.2 Chert types based on internal structures of the chert bands (no matter how long) pinch out laterally. Thin calcarenites are located at the bottom part of long Macroscopically, two dierent textures were dened. chert bands (Figure 6B) and are rarely found at the top. They are granular texture (Figures 6B, 8G and 8H) and Chert bands and calcarenites-calcirudites are surrounded microcrystalline-porcelanious texture (Figures 6B-F, 7B, by calcilutite (Figures 6B and 7A). The Bozburun Hill I 7C, 8K and 8L). The microcrystalline-porcelanious texture Section includes two bands that are 6 m and 4 m long. is the most common texture in the study area. These cherts The Bozburun Hill II Section consists of ve bands, whose have a regular structure and smooth appearance. They are lengths range from 3.2 m to 35 m. The thickness of chert gray colored in the Bozburun Hill I Section (Figure 6E) and bands varies between 7.0 cm and 35 cm (Table 2). milky brown colored in the Bozburun Hill II Section (Fig- Cherts whose length less than three meters are clas- ure 7C). The porcelanious textured cherts are heavily frac- sied as a lens. Chert lenses are divided into two groups tured and cracked (Figures 6D and 6E). based on the number of lenses. The single lens con- The granular textured cherts are seen in the Bozburun tains only one lens (Figures 6E, 6F and 7B), while multi- Hill I Section. This texture has been found in both chert ple lenses comprises two or more combined lenses (Fig- lenses and chert bands. The granular appearance, rough ures 6C, 6D, 7B and 7C). The length of multiple lenses surface and hollow structure of this texture allow easy dif- was measured along the longest axis parallel to horizontal ferentiation from the porcelanious texture (Figure 6B). The plane, and thickness measurements were taken from the thickness of this level is about 10 cm in chert bands. The thickest parts of lenses. Fifteen measurements were taken lower surface of this texture is wavy, while the upper sur- from the Bozburun Hill I Section, and thirty-ve measure- face has a sharp contact with porcelanious textured cherts Occurrences of Chert in Jurassic-Cretaceous Calciturbidites (SW Turkey) Ë 453

Figure 6: The eld photos of chert bearing calciturbidites in the Bozburun Hill I Section. A) The general view of section, chert bearing lev- els are located at the bottom (man in the circle for scale: 1.80 m). B) A chert band with wavy upper and lower surfaces includes a granular chert-lower layer and a porcelanious chert-upper layer. C) The eld view of regularly and irregularly combined and elongated multiple chert lenses (Hammer for scale: 33 cm). D) The eld view of regularly combined and elongated multiple chert lenses. E) The single chert lens with regular view in calcilutite. F) The single chert lens with irregular upper surface in calcilutite. 454 Ë M. Gül

Figure 7: The eld photos of chert bearing calciturbidites in the Bozburun Hill II Section. A) A general view of the section. Chert bearing levels are located at the bottom. A chert band with smooth upper and lower surfaces is located on the left of the gure. B) The eld view of regularly combined and elongated multiple chert lens, the single chert lens and chert lled veins in calcilutite (geologic hammer for scale: 33 cm). C) The regularly combined and elongated multiple chert lenses are located at the upper part of section. The erosion along the chert and calciturbidite level led to determine the continuation of chert level through the calciturbidite (hammer for scale: 33 cm). Occurrences of Chert in Jurassic-Cretaceous Calciturbidites (SW Turkey) Ë 455

(Figure 6B). Its thickness reaches a maximum 20 cm in levels include large fragments of fossil shells (B6 sample chert lens. It has a similar fracture with the porcelanious rudstone similar to the B12 sample; Figures 8C and 8D). textured chert. In all samples (calcilutite-calcarenite level without cherts) micritic calcite minerals were replaced by the microcrys- talline quartz minerals to variable amounts (Figures 8B 3.3 Chert types based on host rock and 8E). The silicication was not xed at the top of Bozbu- run Hill I Section. The silicication also aected the calci- Most of the chert lenses and all of the chert bands are as- turbidites including cherts and calciturbidites located im- sociated with calcarenite and calcirudite. These coarse- mediately at the top of the cherty section. The silicication grained calciturbidites were seen either above or below of calcilutites (without chert) can be interpreted as diage- chert levels (Figurse 6B, 6F, 7B). Sometimes, they are in- netic eects during the epigenetic period. The examined truded chert occurrences (Figure 6C). cherty levels are located inside allochthonous unit. During The rest of chert lenses are distributed in calcilutite- the emplacement of this unit, tectonic forces caused ex- micritic limestone (Figurse 6D, 6E, 7B and 7C). Although cess fracture and cracks. Some cracks have been lled with cherts have fractures at this level, they are tougher than the equitant calcite minerals, locally aected by dolomiti- calcilutite (Figure 7C). In the upper part of Bozburun Hill II zation and silicication (Table 4). However, some younger Section, calcilutite with chert lenses are identied. These cracks that cut chert and calciturbidites were only lled by calcilutite are easily dissolved than chert levels. By this the equitant calcite minerals (Figures 8E, 8F and 8K). In way, the extension of chert through (25-30 cm) the calci- addition, the Bozburun Hill II Section has similar features lutite were measured (Figure 7C). to the Bozburun Hill I Section. The B11 chert sample was taken above the B12 sample. Both of them have similar mineral forms. The bladed and 3.4 Microscopic features of the cherts and equitant large calcite minerals (at the center; the B12 sim- related calciturbidites ilar appearance with the B6; Figures 8C and 8D) were re- placed by the bladed (at the edge) and equitant (at the cen- The microscopic features of thin sections are presented ter) large quartz minerals in same mineral form (Figures 8G in Table 4 and Figure 8. Initially calciturbidites and then and 8H). Rarely, original calcite minerals were found in cherts properties are given. The Table 4 contains rstly this thin section. Moreover, silicication aected dolomite the Bozburun Hill I Section and then Bozburun Hill II Sec- (rhombus) minerals (Figure 8H). The big silica replace- tion samples from bottom to top. The B12 (calciturbidite), ments led to development of macroscopically granular ap- B11 (chert bands lower granular level), B13 (calciturbidite), pearances of chert. The granular appeared level abruptly B14 (chert lens), B9 (chert band), B8 (calciturbidite), B7 passes into the porcelanious chert depending on absence (chert lens), and B6 (calciturbidite) samples were taken of coarse-grained calcite mineral/quartz minerals. from the Bozburun Hill I Section. The B15 (calciturbidite) The B14 (chert lenses; Figures 8K) and B9 (chert band) and B16 (chert lenses) samples were taken from the Bozbu- samples are located above the B13 (calcilutite; Figures 8I run Hill II Section at about the same level (Table 4; Fig- and 8J) sample. Both samples were taken from the porce- ure 8). lanious chert levels, which was found inside the calcilu- The large bioclast (rudist fauna fragments) bearing tite interbedded with small amount of the calcarenites. calciturbidites are situated at the base of Bozburun Hill I Similarly, the sporadic radiolarian fossils were xed in Section. The B12 sample thin section (rudstone) includes both sections (Figure 8K). The rest of thin sections of B9 large rudist shell fragments that contain bladed (on the and B14 samples contain irregular and patchy scattered edges) and equitant-coarse calcite minerals (at the center). micritic calcite and calcite shell fragments. The micro- After this calcarenite and calcirudite level (rudstone-B12 crystalline – cryptocrystalline (?) silica minerals lled the sample), micritic limestones-calcilutites (packed biomi- spaces (black-gray) among the unsubstituted calcite min- crite–packstone/wackestone; B13 sample, Figures 8I and erals (colored patch under cross polarized light or gray 8J; B8 samples, Figures 8E and 8F) were found. These sam- mottling under plane polarized light; Figure 8K). The frac- ples consist of planktic foraminifera and silt sized cal- ture that developed after formation of chert, cut cherts and cite minerals (fragments of the rudist shell). Macroscop- calciturbidites. They are lled with the equitant calcite ically, small amount of calcirudite and calcarenite levels minerals. Towards the upper level of cherty sections, the with variable thickness are found inside the calcilutite B7 (chert lens, Figures 8A and 8B) sample was taken above (Figure 4). The subsequent coarse-grained calciturbidites the B8 sample-calcilutite level (Figures 8E and 8F). The ra- 456 Ë M. Gül Packed biomicrite – rudstone [24–26].ists The are rud- generally found induring the Cretaceous [27]. reef The environment calcarenite evolution is developed depending on high sedimentand input bottom current in hemipelagic[28]. environment The angularbioclasts and points out subangular short transportation. fragments- over, More- Şenel (1997, 2007) suggestednental that slope conti- environment forcording calciturbidite to ac- fossil contentsproperties. and Thus, other calcarenite-calcirudite lithologic opments devel- correspond the higher energetic part of slope or high-sediment input derived from shelf. The presence ofplacement silica of calcite by minerals silica minerals depending showon that diagenesis eect re- [2, 3, 7–11]. Packed biomicrite -[24, 25]. packstone The / fossiliferousGlobotruncana sediments wackestone sp. including are deposited150 m [29]. at This type depths micritic rocks are of deposited in a low-energybase environment [30, and 31]. belowcation wave The in dolomitization cracks and pointcite silici- mineral out during replacement diagenesis [2, ofdolomitization 3, sometimes 7–11]. cal- spread The to all vessels, while silicication is seen asinside an to alteration outside. from sp., and Globigerina sp. and abundant sp. The space among Globigerina Globotruncana Microscopic PropertiesThe pebble sizedments are calcite identied. According to shell type frag- of organism, bladedmostly micritic calcite calcite (matrix) and crystal, cal- Interpretation cite with cleavage are seen. Themineral-quartz silica mineral developments compatible with calcite mineralsseen. are The older veins lledequitant with calcite dolomitic mineralsamounts and small of calcite mineral (shell fragments). The microcrystalline-cryptocrystalline (?) silica replacedminerals. the micritic calcite Globotruncana the main veinssp., contains ties Gray-dark gray rud- ist shellsrock. bearing Light gray color, sty- lolite, ssured and fractured. Calciturbidite (Calcarenite- Calcirudite) Calciturbidite (Calci- lutite) Microscopic properties of the chert and related calciturbidite samples. Sample No TypeB12 of Rocks Bozbu- runSection Hill I Macroscopic Proper- B13 Bozbu- runSection Hill I Table 4: Occurrences of Chert in Jurassic-Cretaceous Calciturbidites (SW Turkey) Ë 457 Packed biomicrite -[24, 25]. packstone The / fossiliferousGlobotruncana sediments wackestone sp. including are deposited150 m at [29]. This depths type micritic of a rocks low deposited - in energy environment and below[30, wave base 31]. The silicication pointseect out on diagenesis sedimentation during epigenetic period [2, 3, 7–11]. Similar mottled viewplete due silicication and to transitional incom- structures be- tween host rock and chert are also determined by Bustillo et al., (2002) in lacustrine carbonates. Sparse biomicrite[24, 25]. The / fossiliferousGlobotruncana sediments dismicrite-wackestone including sp. areof 150 deposited mdeposited at [29]. in depths This abelow type low-energy wave micritic base environmentfragments rocks presence [30, and characterize are reef 31]. front-fore reef environment. The Initially micrite rudist is replacedlarge shell by calcite mineral,the recrystallisation initial step diagenesis eect. of Then,of replacement large calcite by thediagenesis eect) silica [2, is 7]. started (another sp., and sp. bearing biomicrite- Globigerina Microscopic PropertiesThe dominant rock unit is thelaminated, micritic- Globotruncana wackestone. The Interpretation cryptocrystalline microcrystalline (?) - the silica micritic calcite in cherty replaced levels. The unsilicied micritic limestoneare in gray parts color under plane polarized light, and colored, irregularly shaped spots irregularlyblack-and-gray scattered base under on thepolarized cross the light. Calcite-lledthat cut cracks both chert andstone micritic part lime- pointed outof cracks development after sedimentation. Large calcitedirectional minerals cleavagemicritic replaced with calcite crystals the sation bi- – (recrystalli- diagenetic step).minerals replaced The large calcite silica miner- als. ties Stylolite, predomi- nantly gray colored micritic limestone, and burgundyored col- chert. Micriticwith limestone big rudist shell fragments. Calciturbidite (Calci- lutite) Calciturbidite (Calcarenite- Calcilutite) Cont. Sample No TypeB8 of Rocks Bozburun Hill I Section Macroscopic Proper- B6 Bozburun Hill I Section Table 4: 458 Ë M. Gül Packed biomicrite – packstone/wackestone [24, 25]. Similar interpretations of B13 sample can be made for this section. The dolomitization is able to characterizeddiagenetic early development [9]. Alterationdolomite and of calcite both minerals byshow silica that minerals later diagenesis eectsnetic during epige- term [2, 3, 7–11].fossil The shell replacement in of this big granular level appeared chert led level. to development of The presence of radiolarianspart point of continental out slope deeper environmentor high [2, sediment 4–6], input fromformation shelf of break. micritic Trans- calcite tocryptocrystalline microcrystalline- (?) silica minerals indicates di- agenetic eects [2, 3, 7–11]. sp. and Globigerina sp. and abun- Globigerina sp. The space among Globotruncana Microscopic PropertiesThe veins are lled with theequitant dolomitic calcitesmall amount minerals of Globotruncana with Interpretation a the main veinssp., contains and dant calcite mineral (shell fragments). The microcrystallinetalline - silica cryptocrys-calcite replaced minerals. the micritic The rhombus-shaped dolomitecalcite minerals and are seen intion. this Both sec- typestered of minerals by are silicato al- minerals. substituted According mineralquartz type, mineral bladed replacedcite bladed mineral at cal- the side offragments, rudist while shell equitantminerals-quartz big minerals silica are located at the center. A few rounded and radial quartzing bear- radiolarians aremaining portion seen. of Thetains the black and section re- gray con- microcrystalline- cryptocrystalline (?)bearing silica base with minerals an irregularlytered scat- colored micritic limestone spots under the cross-polarizedcoarse-silica light. The minerals replacedcoarse-calcite mineral the (possible shell fragments). The calcite-lledthat cracks cut thelimestone both part chert point out and development of micritic cracks after sedimentation. ties Similar to thesample, B13 light stylolite, graylimestone. micritic White colorincludes matrix grayored col- pebble-sized mottle with granular appearance. locally gray colored chert. Itsitionallycontact has tran- with thelimestone. micritic Calciturbidite (Calci- lutite) Chert band (granular view) Chert lens Burgundy colored Cont. Sample No TypeB16 of Rocks Bozbu- run HillSection II Macroscopic Proper- B11 Bozbu- runSection Hill I B14 Bozbu- runSection Hill I Table 4: Occurrences of Chert in Jurassic-Cretaceous Calciturbidites (SW Turkey) Ë 459 Similar interpretations of thebe B14 made sample for this can microscopically section. viewed Macroscopically and mottlingdepending was on incomplete evolved silicicationpresence and of the residual micritic limestoneunsubstituted [9]. micritic The limestoneored left spots gray col- underlight. the normal planeThe radiolarian polarized ratio is increasing in this section, which shows that environmental conditionsbetter are for living. Similar interpretations of the B14ples and B9 can sam- bescopically and made microscopically viewed forwasseendepending mottling on the this incomplete silicica- section.tion and Macro- the presence ofstone residual [9]. micritic The lime- unsubstitutedleaves micritic gray colored limestone spots under the normal plane polarized light. Microscopic PropertiesA fewbearing rounded radiolarians and were seen.remaining radial portion The of section quartz contains black Interpretation andcryptocrystalline (?) graybearing silica base microcrystalline- with minerals an irregularlytered scat- colored micritic limestone spots under the cross-polarized light. Next to rhombicmicrocrystalline-cryptocrystalline dolomite minerals, (?) silica minerals are found. The rounded and radial quartz bearing radiolarians ratio is around the 15%. The microcrystalline-cryptocrystalline (?) silica mineralscluding bearing a few radiolarians chert and micritic in- limestone were found in thisThe section. silica replaced the micritic section at the edge. ties tled with gray-dark gray colored portion terior, milky brown color of freshface.It has sur- quitefragile structure. a colored outerface, sur- darklight gray gray - fresh colored surface.cream-colored The level containsview due to the mottle gray colored patch. Chert band Cream-colored mot- Chert lens Cream-coloredChert lens ex- Reddish cream- Cont. Sample No TypeB9 of Rocks Bozburun Hill I Section Macroscopic Proper- B7 Bozburun Hill I Section B16 Bozbu- run HillSection II Table 4: 460 Ë M. Gül diolarian content of B7 sample is signicantly higher than during emplacement and/or transportation of the Lycian the B14 and B9 samples. In addition, rhombus-shaped Nappes. Thus, the silicication should be developed dur- dolomite minerals have been determined in this section. ing epigenetic term before the transportation of nappes. The silicication altered to edges and corners of these Two dierent internal structures were xed in chert dolomites. The B16 sample (chert lens; Figure 8L) from the lens and band. The calcite mineral structure of the calci- Bozburun Hill II Section has similar properties with the turbidites is responsible for the chert internal structure. B14 and B9 samples. The granular type internal structures were evolved de- pends on a bladed and equitant large calcite minerals re- placement by quartz with same size (Figures 8G and 8H). 4 Discussion Moreover, distribution of this structure is restricted with big calcite mineral-rudist shell fragments scattering in this sections. The granular chert level abruptly passed into mi- The Babadağ Formation was interpreted as product of the crocrystalline - cryptocrystalline (?) silica bearing porce- slope and basin margin environment according to fossil lanious level depend absence of coarse-calcite minerals. contents and its lithologic features [16, 19]. The base of These two levels can be observed in chert band or lens. The Bozburun Hill I Section contains calcirudite and calcaren- microcrystalline-cryptocrystalline (?) silica bearing porce- ite including the big rudist shell fragments (B12 sample; lanious chert bands (B9 sample) and chert lenses (B14, Table 4; Figure 4). The angularity of fragments attests to B16, B7 samples; Figures 8A, 8B, 8K and 8L) are located a small transportation distance and texturally immature inside the planktic foraminifera bearing calcilutite usu- sedimentation. The rudist fragments were derived from ally associated with calcarenite levels (Figures 8E, 8F, 8I rudist reefs on the shelf. They initially moved to the up- and 8J). The microcrystalline silica replaced micritic lime- per part of slope, then excess (may be periodic) sediments stone in this level. A few radiolarians are also found in this were transported to the lower part of slope. The shallowing level. The existence of radiolarians indicates deeper de- of environment or excess fossil fragments input led to de- positional environment than planktic foraminifera bear- velopment of coarse-grained rudist fragment bearing cal- ing calcilutite (Figures 8A, 8B, 8K and 8L). Association carenite and calcirudite (B6 sample; Figures 8C and 8D). of chert occurrences with calcarenites – calcirudite lev- After each calcarenite-calcirudite level formation, plank- els indicate the importance of coarse-clastics from silica tic foraminifera bearing calcilutite level deposited in low- enrichment uids input and transportation of them (Fig- energy environment near the base of the continental slope ures 4, 5, 6 and 7). Those uids led to the formation of (B13, B8 samples; Table 4; Figures 8E, 8F, 8I and 8J). The chert bands or lenses. They rstly replaced big-shell frag- big calcite minerals replaced micrite (recrystallization) de- ments at the lower part of measured sections (bladed- pending on diagenesis almost in all sections, (B6 sample; equitant calcite; B11 sample lower part). This rst stage Table 4; Figures 8C and 8D). The dolomitization is another silicication might have occurred synsedimentary or im- diagenetic process that aected calciturbidites of the study mediately after sedimentation. Then, the silica saturated area (Table 4; Figure 8H). The silicication (depend on di- uids led to formation of chert lens and chert band in the agenesis) aected only bottom part of the Bozburun Hill I micritic limestone-calcilutite levels. At the same time, this and II Sections. The microcrystalline-cryptocrystalline (?) water caused partial silicication of micritic limestone- or larger silica minerals replaced the calcite mineral de- calcilutite levels without chert band or lens occurrences. pending on their mineral structure (Table 4; Figures 8A, This type of silicication might be interpreted as a prod- 8B, 8G, 8H, 8K and 8L). The silicication led to the de- uct of second stage silicication that produced mottled ap- velopment of chert bands or lens formation depending on pearance in chert band and chert lens due to unsilicied- silica availability. In addition, they caused silicication of unsubstitued micritic limestone-calcilutite levels. calciturbidite without chert formation (Figures 8F and 8J). The silicication has aected only the lower part of The silicication is restricted with cherty calciturbidites the Bozburun Hill sections. The coarse-grained calcitur- and immediately at the top of them. The upper part of bidite alignment, the calcite mineral type and the silica Bozburun Hill I and II sections are not including silici- source are the main controlling factors of the chert occur- cation even similar calciturbidite existence. A great many rences in the study area. The radiolarian abundance is very fractures were seen during petrographic and eld inves- low, so they are not main silica source for the chert forma- tigations. They cut chert and calciturbidites, and include tion. Thus, older quartzite and siliceous volcanic rocks, lo- equitant calcite mineral without dolomitization and silici- cated at the bottom of calciturbidites, are the main silica cation (Figures 8E, 8F and 8K). They must be developed source. The contact between the calciturbidites and older Occurrences of Chert in Jurassic-Cretaceous Calciturbidites (SW Turkey) Ë 461

Figure 8: The micro photos of the thin sections. A) The radiolarian (R) bearing chert lens under the plane polarized light (B7 sample). The gray colored irregular spots are unsilicied residual micritic limestone. B) The radiolarian (R: rounded, radial quartz bearing radiolarian fos- sil) bearing chert lens under the cross polarized light. The gray colored spots in the (A) become colored patches (Ca: residual micritic calcite minerals). The gray-white-black colored microcrystalline quartz mineral (Si) replaced the micritic limestone. C) The micro view of the rudist (Ru) shell fragments bearing calcirudite under plane polarized light (B6 sample is similar to the B12 sample: EqCa: Equitant calcite miner- als). D) The micro view of rudist (Ru) shell fragments bearing calcirudite under cross polarized light. The equitant calcite minerals (EqCa) replaced micritic calcite minerals (MiCa) in the recrystallisation stage of diagenesis. The rudist fragment contains bladed calcite minerals (BlCa). E) The calcite lled veins (CaV; under plane polarized light) cut all units in the area. They are younger cracks. F) The micro view of (E) under cross polarized light. The picture is taken from transition of chert (ch) and micritic limestone (MiCa)–calcilutite. The microcrys- talline quartz (Si) replaced the micritic limestone (MiCa). G) The microview of granular-lower level of chert band under plane polarized light. (Fo: fossil fragments possibly rudist shell; Dol: rhombus dolomite mineral, formed as a result of the dolomitization). H) The equitant silica minerals-quartz (EqSi) replaced equitant calcite minerals at the center. The bladed silica minerals-quartz (BlSi) replaced bladed calcite min- erals at the edge. The microcrystalline silica minerals-quartz (MiSi) replaced microcrystalline calcite minerals. Some fossil fragments (Fo) preserve its colored appearance under cross polarized light depending on low silica input. The silicication also alters dolomite (Dol) min- erals. I) The microview of the Globotruncana sp. (Glt) and the Globigerina sp. (Glb) bearing biomicrite-wackestone (micritic limestone) under plane polarized light. J) The colored big equitant calcite (EqCa) replaced micritic calcite (MiCa) depending on the recrystallization stage of diagenesis. Then black-gray colored silica minerals (Si) replace the equitant calcite (EqCa) depending on the silicication stage of diagene- sis during the epigenetic term. K) The microview of the chert lens with the radiolarians (R) under cross polarized light. The microcrystalline silica minerals-quartz (MiSi) replaced the microcrystalline calcite minerals. The residual, colored fossil fragment (Fo) led to development of mottling view. The dolomite mineral (Dol) is also altered by silica intruding. The younger calcite lled veins (CaV) cut chert lens without any diagenesis eect. L) The micro view of microcrystalline silica minerals-quartz (MiSi) and relatively higher ratio radiolarians (R) bearing chert lens of the Bozburun Hill II Section under plane polarized light. 462 Ë M. Gül silica source rocks was lost during formation and emplace- diagenetic eects were responsible for the occurrences of ment of the Lycian Nappes (Figures 2 and 3). Moreover, the chert. tectonic forces acted during the nappes transportation led The silicication of oolitic limestones (the Mid- to development of numerous calcite lled fractures and Jurassic Camarena Formation) was developed after com- cracks (without any diagenesis eects; recrystallization, paction, cementation, fracturing and local dissolution dolomitization or silicication; Figures 8E, 8F and 8K). [7]. The silicication started to aect host rock from cal- Those cracks cut chert bearing lower calciturbidites and cite cement [7]. Bustillo et al. (1998) determined chert upper calciturbidites without chert. Thus the silicication- occurrences inside the marl-turbidite alternation, which chertication should be completed before the starting of evolved depending on a submergent of platform under the Lycian Nappes transportation (emplacement age the the eect of meteoric water. The source of silica was de- latest Cretaceous to Late Miocene [23]). termined as the radiolarian bearing marls. In our study The chertication of study area shows some similari- area, microcrystalline – cryptocrystalline (?) silicication ties and discrepancies with cherts in other regions. For ex- started from micritic binding materials. However, the ra- ample the peculiar concentric structures of chert, reported diolarian is not interpreted as a main silica source due by Behl (2011) in the Monterey Formation-California, were to its low quantity, older quartzite and siliceous volcanic not seen in this study due to uncompleted silicication. rocks are evaluated as a main silica source. The silici- Previous studies emphasized that chert nodules may form cation of calciturbidites, examined in this study, should by the way of contraction, chemical self-organization dur- be completed before transportation of the Lycian Nappes. ing precipitation or deposition of radiolarians [3, 4]. In It may be that the nappes were submergent during trans- this study, radiolarians are in low abundance, and carry portation and emplacement to south. However, there is no a small importance for chert formation; while the distri- signicant sign of meteoric water eect determined in this bution of coarse-grained calciturbidites is more important study. for chert band-chert lens evolution. Moreover, original cal- The chert nodules of Drunka Formation (Early Eocene) cite mineral form and size also control internal structure of were formed as a result of the replacement of carbonate replacement cherts of the Babadağ Formation. The silici- mud by microcrystalline quartz and replacements of fos- cation, even partially, was determined in all thin sections sils by equate mega quartz, quartzite and chalcedony un- of the lower part of Bozburun Hill Sections, identied that der the eect of the meteoric water diagenesis [8]. The re- silica-rich water circulation present during epigenesis af- crystallization (micritic calcite replaced by equitant calcite fected only the lower part. mineral), rhombus dolomite mineral formation (dolomi- Baumgartner (2013) emphasized that radiolarite tization), and silicication (microcrystalline quartz re- evolved as chert-shale couplets, in Mesozoic stratigraphy placed micritic calcite; equant-blade quartz replaced big of the Neotethyan realm. The fault blocks controlled pa- calcite mineral bearing shell fragments) are the main dia- leogeography of the Western Tethys and led to deposition genetic process, determined in the lower part of calcitur- of the radiolarite, pelagic sedimentation, and deposits on bidite in the Bozburun Hill Sections. the carbonate platform [6]. Moreover, Baumgartner (2013) The Upper Jurassic chert nodules of the Holy Cross mentioned that an earlier suggestion of the radiolarite Mountain occurred within micrites and partially in biomi- deposition below the Calcite Compensation Depth (4-5 km critic or biopelmicritic wackestone [10]. They found small below the sea level) is under debate. Similarly, fault blocks transition zone between chert nodules and host rock. Mi- controlled topography was xed during Triassic-Jurassic gaszewski et al. (2006) suggested that silicication of Up- geologic history of the study area [23]. The Lycian Nappe per Jurassic chert nodules developed synsedimentary or sediments evolved on the rift/passive margin in the north- during early diagenesis (due to sedimentary breccia with ern Neotethys Ocean (separating the Menderes–Tauride embedded chert nodules, convex bottomed and relatively block and Eurasia) [23]. The nappes were emplaced onto at topped concretions, and nodules formed as a result of the southern continental margin from the latest Creta- silicication of bivalves or crustacean burrows). The silici- ceous to the Late Miocene [23]. In the study area, the cation in our study is situated in both biomicrite (wacke- chert band and lens are located inside the calciturbidites. stone, packstone) and packed biomicrite (rudstone). The However there are no regular chert and calciturbidite al- calcarenites and calcirudite developments are determined ternations seen in the study area that pointed out local instead of breccia development. In addition, silicication factors (distributions of calciturbidite, components of cal- in the study area is not limited with coarse-grained level; citurbidite, and orientation of calcarenite-calcirudite) and it is also seen in the calcilutite. Occurrences of Chert in Jurassic-Cretaceous Calciturbidites (SW Turkey) Ë 463

5 Conclusions viewers for their valuable contributions. My great thanks go to Ryan Ickert (language editor) for his valuable contri- butions. The results of this study are listed below. 1. Chert bands (with smooth or wavy surfaces) and chert lenses (single with irregular or regular surface; and multiple lenses with irregularly or regularly combined References and elongated) have been described in Lower Jurassic-

Upper Cretaceous calciturbidites (in SW Turkey). [1] Lapidus F., Winstanley I., Collins Dictionary of Geology, Collins, 2. Initial chert occurrences are associated with calcaren- Glasgow, 565, 1990. ite and calcirudite levels. Some chert occurrences con- [2] Boggs S. Jr., Principles of Sedimentology and Stratigraphy, tain two layered structures: a granular lower part and Macmillan Publishing Company, New York, USA, 771, 1987. porcelanious upper part. The granular level formed [3] Behl R.J., Chert spheroids of the Monterey Formation, California (USA): early-diagenetic structures of bedded siliceous deposits. as a result of the replacement of big equitant and Sedimentology, 2011, 58, 325–351. bladed calcite mineral bearing shell (rudist) frag- [4] Kunimaru T., Shimizu H., Takahashi K., Yabuki S., Dierences in ments with equitant and bladed quartz minerals. The geochemical features between Permian and Triassic cherts from upper porcelanious chert level formed as a result of the Southern Chichibu terrane, southwest Japan: REE abun- the replacement of micritic limestone with microcrys- dances, major element compositions and Sr isotopic ratios. talline quartz. Sediment. Geol., 1998, 119, 195–217. [5] Aiello I.W., Hagstrum J.T., Paleomagnetism and paleogeography 3. A few radiolarian bearing chert occurrences were of Jurassic radiolarian cherts from the northern Apennines of found in calcarenites-calcirudites, and they were also Italy. Geol. Soc. Am. Bull., 2001, 113, 469–481. seen in micritic limestone-calcilutite levels without [6] Baumgartner P.O., Mesozoic radiolarites–accumulation as a chert. The chert occurrences show a mottled appear- function of sea surface fertility on Tethyan margins and in ocean ance due to the presence of unsilicied-unsubstitued basins. Sedimentology, 2013, 60, 292–318. [7] Bustillo M.A., Delgado A., Rey J., Ruiz-Ortiz P.A., Meteoric water micritic limestone. participation in the genesis of Jurassic cherts in the subbetic of 4. The silicication partially aected calcilutite level southern Spain - a signicant indicator of penecontemporane- without cherts. All silicied levels are in the lower part ous emergence. Sediment. Geol., 1998, 119, 85–102 of measured sections. The fractures, lled with calcite [8] McBride E.F., Abdel-Wahab A., El-Younsy A.R.M., Origin of without silicication, evolved during transportation spheroidal chert nodules, Drunka Formation (Lower Eocene), and/or emplacement of the Lycian Nappes (including Egypt. Sedim., 1999, 46, 733–755. [9] Bustillo M.A., Arribas M.E., Bustillo M., Dolomitization and cherty level) and cut cherts and chert bearing calcilu- silicication in low- energy lacustrine carbonates (Paleogene, tites in the lower part, and calciturbidites. Madrid Basin, Spain). Sediment. Geol., 2002, 151, 107–126. 5. The local and partial silicication, as well as the lim- [10] Migaszewski Z.M., Gayuszka A., Durakiewicz T., Starnawska E., ited chert occurrences indicate that silica bearing u- Middle Oxfordian–Lower Kimmeridgian chert nodules in the ids have a limited eect. If the small amount of ra- Holy Cross Mountains, south-central Poland. Sediment. Geol., 2006, 187, 11– 28. diolarian is taken into consideration, older quartzite [11] Bustillo M.A., Chapter 3: Silisication of continental carbon- and silica bearing volcanic rocks, located at the bot- ates. Dev. Sedimentol., 2010, 62, 153–178. tom, are the main silica sources. Moreover, younger [12] Saller A., Ball B., Robertson S., McPherson B., Wene C., Nims R., calcite lled fractures, an absence of meteoric diagen- Gogas J., Reservoir characteristics of Devonian cherts and their esis eects, loss of contact between chert bearing cal- control on oil recovery: Dollarhide Field, West Texas. AAPG Bull., citurbidites, silica sourced older rocks, and limited- 2001, 85, 35–50. [13] Murray R.W., Chemical criteria to identify the depositional en- uncompleted silicication point out that chertication vironment of chert: general principles and applications. Sedi- should be completed during the epigenetic term de- ment. Geol., 1994, 90, 3–4, 213–232. pend on silica rich uid circulation before the trans- [14] Murray R.W., Brink M.R.B.T., Gerlach D.C., Russ III G.P., Jones portation and emplacement of the allochthonous Ly- D.L., Rare earth, major, and trace elements in chert from the cian Nappes. Franciscan Complex and Monterey Group, California: Assessing REE sources to ne-grained marine sediments. Geochim. Cos- mochim. Acta, 1991, 55, 7, 1875–1895. Acknowledgement: The author thanks to Dr. Ulas˛Avs˛ar [15] Wang J., Chen D., Wang D., Yan D., Zhou X., Wang Q., Petrol- and Dr. Özgür Avs˛arfor introducing the eld and Mr. Ali ogy and geochemistry of chert on the marginal zone of Yangtze Aluc˛for his helping during the eld work. I would like to Platform, western Hunan, South China, during the Ediacaran– thank editors especially Jan Barabach and anonymous re- Cambrian transition. Sedim., 2012, 59, 809–829. 464 Ë M. Gül

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