Bull. Min. Res. Exp. (2016) 153:91-111 MINERAL RESEARCHAND EXPLORATION @ |HTAJ Research and Exploration http://bulletin.mta.gov.tr TRACE FOSSILS FROM DEEP SEA SEDIMENTS OF THE LATE EOCENE CEYLAN FORMATION, GELiBOLU PENINSULA (SW THRACE, TURKEY) Huriye Demircana* and Alfred Uchmanb a General Directorate of Mineral Research and Exploration, Department of Geological Research, 06520, Ankara, Turkey b Institute of Geological Sciences, Jagiellonian University, Oleandry 2a; 30-063 Kraków, Poland Research Article Keywords: Turbidites, Basin Plain, Late Eocene, Graphoglyptids, Trace Fossils. Received: 26.01.2016 Accepted: 11.04.2016 ABSTRACT In this study, trace fossils of the Ceylan Formation (Late Eocene) in the area NW of Findikli village and on the coast of the Ece Bay the Gelibolu Peninsula are identified for the first time. They occur in gray siltstones and mudstones intercalated with thin-bedded, parallel and ripple laminated sandstones, which were deposited on a basin plain in proximilt of a slopes in the Thrace Basin. The Late Eocene Ceylan Formation includes pre-depositionl (Belorhaphe zickzack, Desmograpton isp., Helicolithus ramosus, Helminthorhapheflexuosa, Paleodictyon majus, Paleodictyon minimum, Paleodictyon strozzii, Saerichnites isp., Urohelminthoida appendiculata) and post- depositional (Phycosiphon incertum, Spongeliomorpha oraviense, Trichichnus isp., Planolites isp., Ophiomorpha isp., Ophiomorpha annulata, Scolicia isp., Scoliciaprisca, and Thalassinoides isp.) trace fossils. This trace fossil assemblage is typical of the Nereites ichnofacies (Paleodictyon ichnosubfacies), which characterize deep-sea, thin bedded turbididitic sediments oxygenated sea floor. 1. Introduction The Ceylan Formation is a characteristic Late Eocene lithostratigraphic unit of the Thrace Basin in the study area is located in badlands NW of Findikli village and in the coastal cliffs of the Ece Bay (Figure 1A). These areas were studied mainly in terms of stratigraphy and regional geology (Ternek, 1949; Druit, 1961; Onem, 1974; Saltik, 1974; Saner, 1985; Sumengen et al., 1987; Onal, 1987; §enturk and Karakose, 1987; Siyako et al., 1989; Okay et al., 1990; Sumengen and Terlemez, 1991; Erol, 1992; Temel and ęiftęi, 2002; Kesgin and Varol, 2003), palaeontology (Sonmez-Gokęen, 1964, 1973; Gokęen, 1967, 1971, 1972; Tekkaya, 1973; Taner, 1977, 1981, 1983, 1994; Freels, 1980; Toker and Erkan, 1985; Unal, 1996; §afak, 1999; Tunoglu and Unal, 2001a, b). Very few papers refer to ichnology (Demircan, 2008; Demircan and Uchman, 2016). In this paper, trace fossils of the Ceylan Formation are presented and interpreted in reference to palaeoenvironment. 2. General Geology and The Ceylan Formation The Gelibolu Peninsula is built of pre-Cenozoic basement units which are unconformably overlaid by Eocene deposits (Figures 1A-C). In the Gelibolu Peninsula, the pre Cenozoic basement consists of the pre-Maastrichtian ophiolitic complex settled in and Maastrichtian-Paleocene limestones. They are covered by the Lower Eocene deep-sea mudstones and sandstones of the Karaagaę Formation. Generally, this formation shows an increase in grain sizes and bedding thicknesses up the section. The the Karaagaę Formation is overlain conformably by the fluvial red beds of the Early- Middle Eocene Fięitepe Formation. It is covered unconformably by nummulitic-reefal limestones of the Middle Eocene Sogucak Formation, which is locally accompanied by sandstones and conglomerates. Above, the deep-sea Late Eocene Ceylan Formation is present. It is dominated by calcareous, massive mudstones intercalated by turbiditic sandstone- mudstone beds. Contribution of the turbiditic sandstones is higher in the part of the sections studied. The overlying Mezardere, Osmancik and Armutburnu * Corresponding Author: Huriye DEMIRCAN, e-mail: asmin68@yahoo.com.tr http://dx.doi.org/10.19111/bmre.04255 91 Trace Fossils From Deep Sea Sediments Of The Ceylan Formation (SW Thrace, Turkey) formations, with a transition from shales to nearshore sandstone-dominated facies of a deltaic complex mark a regression, which started at the beginning of Oligocene. An extensive volcanism (Hisarlidag- Ayvacik volcanics) predominated during Early-Middle Miocene in the region. Sedimentary deposition that developed during Late Miocene continued until the beginning of Early Pliocene. The Gazhanedere, Kirazli and Alęitepe formations have been formed in this time period. The Pliocene- Quaternary Ergene Formation, which does not outcrop on the land was detected in drills and seismic sections carried out by TPAO. All these units in the study area have then been unconformably covered by Quaternary alluvia (Siyako et al., 1989). The Ceylan Formation was named by Unal (1967), with its type sections in Findikli-1 and Ece Bay-1 in which basin plain deposits were interpreted. In the study area, the Ceylan Formation sediment succession begins with volcanic tuffs and grades up into calcareous, massive mudstones. The tuffs are subdivided into two part: thin bedded and massive tuffs. The thin bedded tuff consists of fine-grained volcanic groundmass which contain mud pieces, Figure 1- A) Location map of the study area. B) Geological map. C) Generalized stratigraphic column of the Gelibolu Peninsula (from Temel and ęiftęi, 2002). 92 Bull. Min. Res. Exp. (2016) 153:91-111 pebble grains and volcanic rock fragments of various sizes. It passes gradually up into bedded and unbedded fine-grained tuffs. These tuffs also grade up into calcareous mudstones, which are rich in carbonates, structureless, and rarely interbedded by thin bedded, granular sandstone layers. The calcareous mudstones gradually pass up into gray massive mudstones, which contain vertical and horizontal trace fossils. In the lower and middle part, they contain intercalations of thin-bedded sandstones, which contribution increases up the section. In average, The Ceylan Formation is 560 m thick, but it the thickness varies from 300 to 600 m depending on the geometry of the basin (Sumengen and Terlemez, 1991). The late Eocene age is based on Pityosporites spp., Triletes sp., Echinatisporites sp., Batiacasphaera sp., Homotryblium plectilum, Diphyes colligerum, Deflandrea phosphoritica, Hystrichokolpoma sp., Ceistosphaeridium sp., Cordosphaeridium sp., chitinous foraminiferal inner walls and the Hypae palynomorph assemblage obtained from the mudstone samples (Bati et al., 2002). The sandstone and shale dominated parts are referred to a deep sea turbiditic system (Kesgin and Varol, 2003). 3. The Studied Sections 3.1. The Findikli-1 section Findikli-1 section is located in the NW part of the Gelibolu Peninsula, along the road between Findikli village and Komur limani (harbor) and gorges SW of the road (GPS coordinates: N40°26.866'; E026°31.700'; ±9 m). (Figures 1A, B). The succession is formed by thin-bedded, fine- grained, turbiditic sandstone-siltstone beds intercalated with turbiditic and hemipelagic calcareous mudstones (Figure 2). The sandstones are parallel and ripple laminated. Lower bedding surfaces of the sandstone beds are rich in semi-reliefs of patterned, meandering, star- and net-shaped invertebrate trace fossils ascribed mainly to graphoglyptids. The trace fossils include (from the bottom to the top) pre-depositional Paleodictyon majus, Helminthorhaphe flexuosa, Urohelminthoida appendiculata, Belorhaphe zickzack, Phycosiphon incertum, Ophiomorpha annulata, Desmograpton isp., Saerichnites isp. and post-depositional Figure 2- The Ceylan Formation in the Findikli-1 section. A) The outcrop with sandstones containing graphoglyptids of the Ceylan Formation (Findikli village). B) Thin-bedded sandstone intercalations in calcareous mudstones in the lower part of the gorge. Spongeliomorpha oraviense and Thalassinoides isp., which occur on the lower bedding surfaces of the thin- and medium-bedded sandstone beds. Moreover, the trace fossils Trichichnus isp., Phycosiphon incertum are present in the gray mudstones (Figure 3). 3.2. The Ece Bay-1 section The Ece Bay-1 (Ece Limani-1) section is located in the cliffs of the Ece limani coast, in the NW part of the Gelibolu Peninsula (GPS coordinates: N40°21.810'; E025°19.710'; ±9 m) (Figures 1-A, B). The succession is formed by gray mudstone intercalated with thin-bedded, fine-grained sandstone beds (Figure 4). In the mudstones, Trichichnus isp., was recognized. The sandstone beds contain Thalassinoides isp., Planolites isp., Ophiomorpha annulata, Scolicia isp., Scolicia prisca (rare), Helminthorhaphe flexuosa, Phycosiphon incertum and Helicolithus ramosus (formerly known as Punctorhaphe paralella) (Figure 5). 93 Trace Fossils From Deep Sea Sediments Of The Ceylan Formation (SW Thrace, Turkey) Figure 3- The Findikli-1 measured section with trace fossil distribution. 4. Trace Fossils The section were studied “bed-by-bed”, with registration of lithology and trace fossils, which were documented by photography, mostly in place. Nineteen ichnotaxa are have been recognized in the study area. Their more extensive is in the monographs and papers by Hantzschel (1975), Książkiewicz (1977), Seilacher (1977), Fillion and Pickerill (1990), Crimes and Crossley (1991) and Uchman (1998). 4.1. Simple and Branching Structures This group consists of mostly tubular, variable oriented structures, formed mainly by “worms” and “crustaceans” (e.g., Książkiewicz, 1977; Demircan and Toker, 2003). Planolites Nicholson, 1879 Planolites isp. Description: Horizontal, hypichnial, tubular structures, without wall, 2-4 mm in diameter. 94 Bull. Min. Res. Exp. (2016) 153:91-111 Figure 4- The Ceylan Formation in the Ece Bay-1 section A) General view of the Ceylan Formation outcrops along the Ece limani coast. B, C) Intercalations of sandstone and siltstone beds in fine in mudstones. Remarks: Planolites occurs in a great variety of facies and is formed mainly by deposit-feeding “worms” (Pemberton and Frey, 1982). It ranges from the Precambrian to the Recent (Hantzschel, 1975). Ophiomorpha Lundgren, 1891 Ophiomorpha isp. (Plate III, Figure B) Description: Horizontal, hypichnial, tubular structures, with a wall, preserved in full relief, 8-9 mm in diameter, traced for a distance up to 60 mm. Remarks: The described Ophiomorpha isp., resembles Ophiomorpha rudis Książkiewicz, 1977 (Uchman, 1991, 2009). Ophiomorpha, produced mainly by decapod crustaceans, can intergrade with Thalassinoides, Spongeliomorpha and Gyrolithes (e.g., Kennedy, 1967; Fursich, 1973; Bromley and Frey, 1974; Kern and Warme, 1974. Ophiomorpha annulata (Książkiewicz, 1977) (Plate I, Figure A) Description: Mainly horizontal, tubular structure with a wall, 3.3 mm wide, observed on the distance up to 40 mm. Remarks: This ichnospecies was described under Granularia Pomel or Sabularia simplex Książkiewicz, 1977) but it was included in Ophiomorpha (Uchman, 1995; Tunis and Uchman, 1996 a,b). Saerichnites Billings, 1866 Saerichnites isp. (Plate I, Figure B) Description: A group of hypichnial hemispherical mounds, approximately 8.3 mm in diamneter. Remarks: Saerichnites Billings, 1866 (see also Hantzschel, 1975) has then been interpreted by Uchman (1995) as casts of shafts connecting a burrow system with the sea floor. Spongeliomorpha oraviense (Książkiewicz, 1977) (Plate I, Figure C) Description: A short, tubular structure covered by oblique short ridges, about 10 mm in diameter. Remarks: This trace fossil was described under Halymenidium by Książkiewicz (1977) and was included in Spongeliomorpha by (Uchman, 1998). 95 Trace Fossils From Deep Sea Sediments Of The Ceylan Formation (SW Thrace, Turkey) Figure 5- The Ece Limani-1 measured section with distribution of trace fossils. 96 Bull. Min. Res. Exp. (2016) 153:91-111 The ridges are interpreted as casts of scratch marks of crustaceans. Thalassinoides Ehrenberg, 1944 Thalassinoides isp. (Plate I, Figures D, E) Description: Mostly horizontal, tubular, branched burrows, about 10 mm in diameter. They show Y- and T-shaped branches. They form three- dimensional burrow systems, which include shafts connecting the horizontal parts with the sediment surface. Remarks: Thalassinoides is produced mainly by crustaceans, typically in shallow-marine environments, but also in the deep sea (Frey et al., 1984; Ekdale, 1992). According to Follmi and Grimm (1990), the Thalassinoides crustacean tracemaker can survive transportation by turbiditic currents and make burrows even in anoxic conditions for a limited time. Thalassinoides, widely distributed in the Mesozoic and Cenozoic, occurs also in shallow-water sediments in the Paleozoic (e.g., Palmer, 1978; Archer and Maples, 1984; Sheehan and Schiefelbein, 1984; Stanistreet, 1989; Kulkov, 1991). Large tubular burrow (Plate I, Figure F) Description: Horizontal, cylindrical structure, 27-30 mm in diameter, without branches. Remarks: Usually, such large burrows are mainly formed by crustaceans in shallow-marine environments (Frey et al., 1984), but they can occur also in turbiditic systems (Uchman, 1991). Trichichnus Frey, 1970 Trichichnus isp. (Plate II, Figure A) Description: Branched or unbranched, thread- like, cylindrical, straight or slightly winding structure, filled with pyrite or iron oxides, variable oriented, less than 1 mm in diameter. Remarks: Trichichnus, formed by opportunistic organisms, was discussed by Fillion and Pickerill (1990) then by Uchman (1995, 1999). It is interpreted as a structure formed by sulphur bacteria in the transition between anoxic-dysoxic sediments (Kędzierski et al., 2015). 4.2. Winding and Meandering Structures The studied trace fossils ascribed to this group include horizontal structures produced by irregular echinoids (Scolicia) and some graphoglyptids produced by small, unknown invertebrates. Scolicia de Quatrefages, 1849 Scolicia isp. (Plate II, Figure B) Description: Hypichnial, trilobate, curved or meandering ridge, 25-30 mm wide. Remarks: Scolicia is formed by irregular echinoids (Uchman, 1995) and ranges from Late Jurassic to Recent (Tchoumatchenco and Uchman, 2001). Scolicia prisca de Quatrefages, 1849 (Plate II, Figure C) Description: Epichnial, trilobate, curved or meandering furrows, 15-25 mm wide and up to 3.5 mm deep. The middle lobe is convex up and 6 mm wide, covered with perpendicular ribs. The lateral lobes are covered by oblique ribs. Remarks: This ichnospecies is formed by irregular echinoids at the transition between sandstone and mudstone within turbiditic beds (Uchman, 1995). It ranges from Late Jurassic to Recent (Tchoumatchenco and Uchman, 2001). Helminthorhaphe Seilacher, 1977 Helminthorhaphe flexuosa Uchman, 1995 (Plate II, Figures D-E) Description: Hypichnial meandering strings in fine-grained sandstones. The strings are 1.5-2 mm in diameter and the meanders are 55-60 mm deep and 2-3 mm wide, without bulges in the turns. Remarks: This is graphoglyptid burrow produced by unknown worms, described also Helminthorhaphe crassa (see Seilacher, 1977). 97 Trace Fossils From Deep Sea Sediments Of The Ceylan Formation (SW Thrace, Turkey) Helicolithus ramosus (Vialov, 1971) (Plate II, Figure F; Plate III, Figure A) Description: Hypichnial, tight meanders composed of aligned knobs, 0.8-1.0 mm in diameter, 1.5-2.0 mm. Remarks: The aligned knobs are casts of shafts connecting spiral string arranged in meanders (Tunis & Uchman, 1996b). Helicolithus ramosus ranges from the Senonian (Książkiewicz, 1977) to the Miocene (D’Alessandro, 1980. 4.3. Branched Winding and Meandering Structures Belorhaphe Fuchs, 1895 Belorhaphe zickzack (Heer, 1877) (Plate III, Figure B) Description: Hypichnial semi-relief zigzag meanders in fine grained turbiditic sandstones. The turning points of the zigzag are enlarged and are 5 mm wide. The zigzag turnsat the angle of approximately 50°. The string is 1.0-1.5 mm wide. Remarks: Belorhaphe zickzack ranges from the Beriassian (Książkiewicz, 1977) to the Oligocene (Nowak, 1970) and occurs mainly in deep marine clastic sediments. Desmograpton Fuchs, 1895 Desmograpton isp. (Plate III, Figure C) Description: Hypichnial rows parallel to sub- parallel ribs in fine grained turbiditic sandstones, preserved in semi-relief. The ribs are curved, their relief is semicircular od asymmetrically oval. The ribs are 5.5-6.0 mm, 1-1.5 mm wide. Remarks: Desmograpton is a typical three dimensional graphoglyptid (Seilacher, 1977) showing a series of preservational variants (Uchman, 1995). It ranges from the Silurian (McCann, 1989, 1993) to the Miocene (D Alessandro, 1980; Uchman, 1995). Urohelminthoida Sacco, 1888 Urohelminthoida appendiculata (Heer, 1877) Description: Hypichnia meanders with protrusions in the turning points of the meanders, preserved in semi-relief in fine grained turbiditic sandstones. The string is undulating, 2 mm wide, and the meanders are 35-40 mm deep and 4 mm wide. Remarks: This is a typical graphoglyptid (Seilacher, 1977; Uchman, 1995). 4.4. Networks Structures Paleodictyon majus Meneghini in Peruzzi, 1880 (Plate III, Figure E) Description: Hypichnial hexagonal nets in fine- grained turbiditic sandstones. Meshes of the net are 6.0-7 mm wide and the string is 0.5 mm wide. Remarks: This is common ichnospecies of Paleodictyon in Cenozoic turbidites (Książkiewicz, 1977). Paleodictyon, a typical graphoglyptid, is interpreted mainly as a farming structure (Seilacher, 1977), produced mostly in the deep-sea sediments, occasionally occurring in shelf sediments in the Paleozoic (Archer and Maples, 1984; Paczesnia, 1985) and in the Mesozoic (Hantzchel, 1964; Gierlowski-Kordesch and Ernst, 1987; Hantzpergue and Branger, 1992). Paleodictyon stratigraphically ranges from the Cambrian (Crimes and Anderson, 1985; Pacześna, 1985) to Recent (Ekdale, 1980; Miller, 1991). Paleodictyon minimum (Sacco, 1888) Description: Hypichnial net composed of a string which is 0.25-0.3 mm wide and arranged in meshes which are1-2 mm wide. Remarks: This ichnospecies is known mostly from Cenozoic turbidites (e.g.,Kindelan, 1919; Vialov & Golev, 1965). Paleodictyon strozzii Meneghini in Savi & Meneghini, 1850 (Plate III, Figures D, E) Description: Hypichnial hexagonal nets in fine grained turbiditic sandstones. Their strings are 0.5-1.0 mm wide and the meshes are 3.6-4.5 mm wide . Remarks: Individual meshes are of different size and can be elongated. 98 Bull. Min. Res. Exp. (2016) 153:91-111 4.5. Spreite Structures Phycosiphon incertum Fischer-Ooster, 1858 (Plate III, Figure F) Description: Small, horizontal lobes encircled by meandering marginal tunnel. The lobes are 1-3 mm wide and up to 10 mm long. The marginal tunnel is about 1 mm wide. Remarks: Phycosiphon incertum is generally formed by sediment-feeders in the early stage of colonization of turbiditic fine-grained sediments (Wetzel and Uchman, 2001; Uchman et al,. 2004). For discussion of this trace fossil see Wetzel and Bromley (1994). 5. Discussion Taking the morphological characteristics of the trace fossils into consideration, the determination of the trace fossil assemblages in the sections studied, composed of pre-depositional Belorhaphe zickzack, Desmograpton isp., Helicolithus ramosus, Helminthorhaphe flexuosa, Paleodictyon majus, Paleodictyon minimum, Paleodictyon strozzii, Saerichnites isp., Urohelminthoida appendiculata and post-depositional Phycosiphon incertum, Planolites isp., Ophiomorpha isp., Ophiomorpha annulata, Scolicia isp., Scolicia prisca, Spongeliomorpha oraviense, Trichichnus isp., and Thalassinoides isp. is typical of the Nereites ichnofacies; the high contribution of graphoglyptids points to the Paleodictyon ichnosubfacies, which is characteristic of thin-bedded sandy turbidites in different parts of depositional systems (Uchman & Wetzel, 2012). The turbidites studied formed in the basin plain or the lower slope, probably in fringes of small fans or isolated lobes. The trace fossils, especially these formed without permanent connection to the sea floor (Planolites, Phycosiphon, Scolicia), indicate good oxygenation in pore waters. Acknowledgement This study has been carried out within scope of the project “Guney Marmara Bolgesinde (ęanakkale- Armutlu Yarimadasi-Balikesir (GB Marmara)-Edremit Korfezi Arasinda Kalan, Gelibolu Yarimadasi) Yuzeyleyen ęokellerin iz Fosillere Dayali Ortamsal Yorumu ve Paleoekolojik Degerlendirilmesi” (Environmental Interpretation and Paleoecological Assessment of Deposits Outcropping in the Southern Marmara Region (between ęanakkale (Dardanel)- Armutlu Peninsula (SW Marmara), Gelibolu Peninsula) based on Trace Fossils) coded as MTA 2012-30-14-08-4/2013-30-14-19. References Archer, A.W., Maples, C.G. 1984. Trace fossil distribution across a marine to nonmarine gradient in the Pennsylvanian of South Western Indiana. Journal of Paleontology 58, 448-466. 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Palaeogeography, Palaeoclimatology, Palaeoecology 168, 171-186. 103 Bull. Min. Res. Exp. (2016) 153:91-111 PLATE 105 Trace Fossils From Deep Sea Sediments Of The Ceylan Formation (SW Thrace, Turkey) PLATE -I A - Ophiomorpha annulata Hypichnial full reliefs in a fine grained turbiditic sandstone bed (Findikli-1 section). B - Saerichnites isp. Hypichnial semi-reliefs in a fine-grained turbiditic sandstone bed (Findikli-1 section). C - Spongeliomorpha oraviense Hypichnial full relief in a fin-grained turbiditic sandstone bed (Findikli-1 section). D, E - Thalassinoides isp. Hypichnial full reliefs in a fine-grained turbiditic sandstone bed (Ece Bay-1 section). F - Large tubular burrow Hypichnial full relief in fine-grained turbiditic sandstone bed (Ece Bay-1 section). 106 Bull. Min. Res. Exp. (2016) 153:91-111 PLATE I 107 Trace Fossils From Deep Sea Sediments Of The Ceylan Formation (SW Thrace, Turkey) PLATE - II A - Trichichnus isp. Endichnial full relief in calcareous mudstone (Ece Bay-1 section). B - Scolicia isp. Hypichnial full relief in a fine-grained turbiditic sandstone bed (Ece Bay-1 section). C - Scolicia prisca Originally, full relief; its lower part is seen at the top of a turbiditic sandstone bed (Ece Bay-1 section). D, E - Helminthorhaphe flexuosa Hypichnial semi-relief in a fine-grained turbiditic sandstone bed (Ece Bay-1 section). F - Helicolithus ramosus Hypichnial semi-relief in a fine-grained turbiditic sandstone bed (Ece Bay-1 section). 108 Bull. Min. Res. Exp. (2016) 153:91-111 PLATE II 109 Trace Fossils From Deep Sea Sediments Of The Ceylan Formation (SW Thrace, Turkey) PLATE - III A - Helicolithus ramosus Hypichnial semi-relief in a fine-grained turbiditic sandstone bed (Ece Bay-1 section). B - Belorhaphe zickzack and Ophiomorpha isp. Hypichnial semi-relief (Belorhaphe) and hypichnial full relief (Ophiomorpha) in a fine-grained turbiditic sandstone bed (Findikli-1 section). C - Desmograpton isp. Hypichnial semi-relief in a fine-grained turbiditic sandstone bed (Findikli-1 section). D - Paleodictyon strozzii Hypichnial semi-relief in a fine-grained turbiditic sandstone bed (Findikli-1 section). D - Paleodictyon strozzii and Paleodictyon majus Hypichnial semi-reliefs in a fine-grained turbiditic sandstone bed (Findikli-1 section). F - Phycosiphon incertum Endichnial full relief in a fine grained turbiditic sandstone bed (Findikli-1 section). 110 Bull. Min. Res. Exp. (2016) 153:91-111 PLATE III 111