Age, composition and paleoenvironmental signi
ficance of a Late Pleistocene
eolianite from the western Black Sea coast of Turkey
Ahmet Evren Erginal
a,*, Na
fiye Gunec Kiyak
b, Yunus Levent Ekinci
c, Alper Demirci
c,
Ahmet Ertek
d, Timur Canel
eaDepartment of Geography, Ardahan University, Ardahan TR-75000, Turkey bDepartment of Physics, Isik University, Istanbul TR-34980, Turkey
cDepartment of Geophysical Engineering, Çanakkale Onsekiz Mart University, Çanakkale TR-17020, Turkey dDepartment of Geography, Istanbul University, Istanbul TR-34459, Turkey
eDepartment of Physics, Kocaeli University, Kocaeli TR-41380, Turkey
a r t i c l e i n f o
Article history:
Available online 26 April 2012
a b s t r a c t
On the basis offield observations, thin section interpretations, microanalytical data, electrical resistivity survey and luminescence dating, the age, composition and internal structure of coastal eolianite on the west Black Sea coast at S¸ile, Istanbul, was studied for a combined interpretation of dune rock develop-ment and facies characteristics. Results demonstrate that the eolianite is made up of south-dipping, large-scale dune stratification, consisting mainly of quartz sand and, in particular, abundant ooids, as well as the binding cement which is composed of calcite and aragonite. Based on Electrical Resistivity Tomography (ERT) images, the eolianite has a thickness of between 3.5 m and 8 m and overlies a buried rugged topography that has developed on the Pliocene unit. This suggests the predominance of northerly winds that account for the landward removal of dune sands by offshore wind drift prior to carbonate cementation. Optically Stimulated Luminescence (OSL) dating estimations revealed that the initial deposition of the laminated eolianite layers on the underlying older unit took place at 138.57 13.65 ka, matching the Karangatian highstand or Marine Isotope Stage (MIS) 5e.
Ó 2012 Elsevier Ltd and INQUA. All rights reserved.
1. Introduction
Quaternary eolianites, which result from carbonate-cemented wind-blown sands in coastal zones, are of profound importance not only in understanding eolian processes that prevailed on the backshore during depositional history but also changes in sea-level during Late Pleistocene and Holocene (Fairbridge and Johnson, 1978;Kelletat, 1991). Recently,Brooke (2001)looked at the global distribution of eolianite and plotted 82% of eolianite exposures on the world’s coasts within latitudes 20 and 40 of both
hemi-spheres, pinpointing common exposures on the coast of Australia, South Africa, the Bahamas and Bermuda as well as several parts of the Mediterranean (Brooke, 2001; Frébourg et al., 2008). Never-theless, only a few records have been documented from Turkish coasts (Kiyak and Erginal, 2010;Erginal et al., in press).
This study presents data on a newly-found eolianite exposed on the west coast of the Black Sea, Turkey, which has not yet been
studied in detail. The nature of the eolianite is described, based on field observations, thin section interpretations, energy dispersive ray spectroscopy/scanning electron microscopy (EDX/SEM) and x-ray diffraction (XRD) data. Then, the deposition age of the eolianite is examined based on optically stimulated luminescence (OSL) dating method. Additionally, in order to delineate the subsurface and internal structure of the eolianite body as well as its contact relationship with the underlying Pliocene unit, an Electrical Resis-tivity Tomography (ERT) survey was also carried out.
2. Material and methods 2.1. Study area
The studied eolianite is located about 13 km west of the S¸ile district of the city of Istanbul, Kocaeli Peninsula, northwest Turkey (Fig. 1a and b). The outcrop lies at 411105300N, 292604600E and is located behind a gravelly sandy beach (Fig. 1c) characterized by abundant bioclastic debris, including Donax trunculus, Venus gallina, Ostrea edulis and Mytilus edulis, and a small quantity of pebbles comprised of andesite, arkose and limestone derived from the
Pre-* Corresponding author.
E-mail address:aerginal@gmail.com(A.E. Erginal).
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Neogene basement rocks of the Kocaeli Peninsula (Abdüsselamoglu, 1963;Yigitbas¸ et al., 2004). In a geomorphological sense, the area forms the northernmost extent of the so-called Kocaeli peneplain with an average elevation of 150e200 m (amsl) and constitutes the main morphological feature between the Black Sea and Sea of Marmara (Ertek, 1995;Yılmaz et al., 2010). Pliocene sediments of terrestrial origin, consisting of interbeds of clay, gravel and lignite, dominate the geology of the area (Okay, 1948). The underlying clays are red and nonfossiliferous, forming a basal unit of Pliocene deposits (Fig. 1d). Based on climatic data from S¸ile Meteorology Station (41100N, 29360E), the area receives an annual precipitation of 749 mm. The long-term average temperature value is 8.5 C.
North-easterly winds dominate throughout the year. Alongshore currents are from the east to the west and the tidal range is not more than 9 cm (Defant, 1961).
2.2. Sampling and microanalyses
Six samples of eolianite were taken from a 5-m-thick coastal exposure at 1 m intervals for thin section study, microanalysis and luminescence (OSL and TL) age determination. Sampling locations are shown inFig. 1d. Thin sections were prepared for petrographic determinations using a Chebios microscope. The elemental composition of both eolianites and rhizoliths was examined using
Fig. 1. Study area. (a, b) Location map, (c) simplified geomorphologic maps, (d) sampling sites (numbered downwards) from thickest outcrop of studied eolianite, (e) SWeNE trending ERT survey lines on Google earth image.
an A Phillips XL-30 S FEG Scanning Electron Microscope equipped with EDX detector. X-ray Diffractometry (Phillips X’Pert Pro) anal-yses were applied to the same samples for mineral determination. The analyses were performed in the Materials Research Centre of Izmir Institute of Technology, Turkey. Total CaCO3% contents were
determined using a Scheibler calcimeter (Schlicting and Blume, 1966). The stable isotope (
d
13C andd
18O) determinations of eolianite carbonates were carried out in Environmental Isotope Laboratory, Geosciences Department, University of Arizona. Anal-yses ofd
18O andd
13C were measured using an automated carbonate preparation device (KIEL-III) coupled to a gas-ratio mass spec-trometer (Finnigan MAT 252).2.3. ERT survey
The ERT survey was carried out with an ARES multi-electrode resistivity meter using dipoleedipole electrode array with 9 data levels along three lines (Fig. 1e). The length of the lines was 110 m with electrodes spaced every 5.5 m. Location of the ERT lines was determined based on the thickest eolianite outcrop on the under-lying Pliocene unit. Processing of the measured data was conducted by tomographic inversion software RES2DINV (Loke and Barker, 1996). The aim of the optimization is tofind a resistivity distribu-tion that agrees with the measured data, thereby minimizing the difference between the measured and calculated data using an iterative scheme. As a sharp resistivity contrast between eolianite body and the Pliocene unit was expected, the blocky (L1 norm)
inversion scheme was used to minimize the sum of the absolute (Abs.) values of the spatial changes in the model resistivity, as suggested in previous studies (Olayinka and Yaramancı, 2000;Loke et al., 2003). The inversion process produced model resistivity tomograms after 5 iterations with Abs. errors of 1.02%, 1.06% and 3.04% for ERT1, ERT2 and ERT3, respectively. Based on the low Abs. errors, the inversion processes were considered to have produced geoelectrical models that approximated a realistic representation of the true resistivity distribution of the subsurface.
2.4. OSL measurements and equivalent dose (De) estimate
All luminescence measurements were performed with an automated Risø TL/OSL reader, model TL/OSL-DA-15, equipped with an internal90Sr/90Y beta source (w0.1 Gy s1), blue light emitting diodes (LEDs) (470 nm, w40 mW cm2) and IR LEDs (880 nm, w135 mW cm2). Luminescence signals were detected using an
EMI 9635QA photomultiplier tube fitted with 7.5 mm-thickness Hoya U-340filters (Bøtter-Jensen, 1997).
The equivalent dose (De) accumulated in quartz grains was
estimated using the conventional single-aliquot regenerative-dose protocol (OSL-SAR), based on a comparison of the natural OSL signal with regenerative OSL signals produced by known laboratory doses (Murray and Mejdahl, 1999;Murray and Wintle, 2000). Using the corrected luminescence signal dose points, a growth curve was constructed and the natural signal was interpolated onto the growth curve to obtain the accumulated dose De (Fig. 2a). The
corrected experimental points on the growth curves for all samples fit well using an exponential function, and the equivalent dose was measured before saturation.
2.5. Dose rate estimation
The annual dose of the radiation environment was estimated using the concentrations of major radioactive isotopes of the uranium and thorium series, and potassium. Radionuclide concentrations in the sediment samples were measured as 111 Bq/kg for U-238; 16 1 Bq/kg for Th-232, and 108 10 Bq/kg
for K-40 using high resolution gamma spectrometry. Over time, carbonate-cemented deposits experience accumulation as well as dissolution of carbonate material as a pore-filling substance. Nathan and Mauz (2008) suggested dose rate corrections for carbonate-rich sediments similar to those for water and organic components, under the assumption that interstitial material is inert. Down core variations of both organic as well as carbonaceous components are presented inFig. 2b. The burial dose rates obtained ranged from 0.66 0.02 to 0.82 0.03 mGy/a and are presented in Table 1. Only beta and gamma dose rates were taken into account for this study. Alpha radiation was ignored due to the short pene-tration of alpha particles and very low internal radioactivity of quartz grains. Dose-rate calculations were made using the conversion factors ofAdamiec and Aitken (1998).
3. Results and discussion
3.1. Facies and subsurface characteristics
The studied eolianite crops out near Alacali village, S¸ile and rests unconformably upon Pliocene sandy clays with 2 m exposed thickness. The visible thickness of the eolianite is 5 m, consisting entirely of southward (leeward)-inclined greatly indurated laminae (Fig. 3a). Its seaward-facing surface is rather rough due to weath-ering holes or downward tapweath-ering pipes, which penetrate down to w5 m in depth from the rock surface. The transition between Pliocene clays and eolianite is well defined and marked by a nearly-horizontal plane (Fig. 3b).
Thin section images show that the rock is tightly-cemented ooid-rich grainstone in composition based on Dunham (1962) classification. In addition, the total amount of CaCO3 may range
between 65% and 95% (Table 2). Its connective cement filling intergrain pore spaces are rather compact and may reach 250
m
m thickness, as understood from the spaces left by dislocated ooid grains. Based on EDX (Table 2) and XRD analyses results, respec-tively, this cement comprises several elements (Wt%) in descending order of Ca> O > C > Si > Na > Fe > Mg ¼ K > Al and the minerals calcite and aragonite. Stable isotope analysis results obtained from the bulk carbonate offive samples demonstrated thatd
13C(&PDB) values vary between1.9 and 7.5 with an average value of 5.3. Thed
18O(&PDB) values, on the other hand, range from 6.3 to 8.3 with an average of w7.5&. These results reveal enrichment in lighter isotopes during meteoric cementation conditions, as confirmed by meniscus type of connective cements (Fig. 3c).The ooids form the main diagnostic feature of the studied eolianite. It is understood that such radially-arranged crystals could be indicative of a high-energy shoal marine deposition environment (Qi and Carr, 2006) and are known to form a significant part of the specific sedimentary facies patterns from the last interglacial coastal deposits (Bardaji et al., 2009). Arranged around angular nuclei formed of calcite and quartz, the concentric layers are mostly circular and ellipsoid in shape. The diameters of concretions vary between 250
m
m and 500m
m (Fig. 3c and d). The fact that the ooids comprise tangentially-oriented crystals in all samples suggests high-energy conditions (Loreau and Purser, 1973), which is confirmed by the common presence of broken ooids, revealing physical deformation by wave or wind effects during removal from the deposition area to the beach or dunes. The thicker ooid envelope in proportion to the size of the nuclei is similar to both recent and MIS 5e deposits in some of the Mediterranean ooids (Bardaji et al., 2009).Even though the sequence does not show a cross-bedding struc-ture typical of carbonate-cemented fossil dune deposits accumulated by bi-directional winds, it preserves some evidence of an eolian origin, such as well-sorting in grain sizes and, particularly, the pres-ence of rhizoliths as terrestrial-sourced organosedimentary
A.E. Erginal et al. / Quaternary International 296 (2013) 168e175 170
components (Fig. 3e). Based on the morphotyphical classification of Klappa (1980), rhizoliths embedded within the eolianite from the surface to a depth of 3 m in the sequence are all in the form of root casts. Looking at them from the inside to the outside, XRD showed that the studied rhizoliths consist of calcite in the inner core (presumably the original location of decayed roots), quartz and calcite in the middle ring, and a mixture of quartz, aragonite and calcite within the encircling outer crust (Fig. 3f). The abundance of calcite as well as aragonite, implying a carbonaceous rhizolith, is suggestive of precipitation by virtue of effective evaporation in dry conditions (Cohen, 1982;Kraus and Hasiotis, 2006), which might have domi-nated after wetter periods allowing plant colonization (Alonso-Zarza et al., 2008) prior to root decomposition and subsequent calcification. The
d
13C andd
18O composition of rhizolith carbonates rangedaround10 as similar to the host rock eolianite, suggesting enrich-ment by meteoric waters after deposition of carbonates.
Regarding the nature of paleotopography buried by the eolian sands, ERT images obtained along three different transects of 110 m length demonstrated a clear transition between the eolianite and underlying Pliocene unit. The measured apparent resistivity pseudosections of three ERT lines are shown respec-tively in Fig. 4(aec). High apparent resistivities located at the uppermost part of the sections represent the eolianite body. Inverse model resistivity sections are illustrated inFig. 5(aec). The NE-SW trending resistivity tomograms displayed a depth range of w12 m. Resistivity contrast between the two units can be clearly seen in three resistivity images. The eolianite unit was distinctly identified in the inverse model sections as having high resistivities in proportion to the underlying Pliocene unit, defined by low resistivities. ERT images reveal that the thickness of the eolianite varies between 3.5 m and 8 m. Even though sections ERT1 and ERT2 reflect a sharp contact between the two units, ERT3 shows a gradual transition in depth. The latter also displays the existence of a possible small buried valley which cuts through the under-lying unconsolidated sandy unit. Thus, resistivity tomograms show a rugged topography at a depth of 5e9 m, fossilized by the eolianite sands. The landward extension of the eolianite decreases from east to west, likely indicating the original extension of the
Table 1
OSL-SAR ages and equivalent doses for samples from different profiles. Sample Depth (cm) OSL ages (ka) OSL dose (Gy) n* Dose rate (Gy/ka) SLE-01 10 112.63 5.15 92.59 2.31 6 0.82 0.03 SLE-02 100 131.40 5.67 97.27 2.72 14 0.74 0.02 SLE-03 200 133.98 7.49 96.45 4.33 20 0.72 0.02 SLE-04 300 136.60 8.16 95.47 4.70 19 0.70 0.02 SLE-05 400 138.11 10.57 94.46 6.46 16 0.68 0.02 SLE-06 500 138.57 13.65 90.88 8.38 7 0.66 0.02 * Number of aliquots measured.
Fig. 2. (a) Growth curve for corrected OSL signals from representative sample SLE-02. Open diamond indicates corrected natural dose point on growth curve, interpolated to horizontal axis to obtain equivalent dose De. Insect OSL signals of eolianite samples, (b) Down core variation of organic and carbonaceous component.
Table 2
Analysis results from studied eolianite samples. The units for element concentrations are Wt%.
Sample code Depth (cm) CaCO3(%) d13C (& VPDB) d18O (& VPDB) Elements (Wt%)
Na Mg Al Si K Ca Fe Cu SLE-02 100 68.1 1.9 6.3 0.36 0.49 1.66 4.53 0.3 31.31 1.71 0.2 SLE-03 200 65.9 6.1 8.3 0.39 0.49 2.27 5.17 0.34 29.63 2.14 0.19 SLE-04 300 55 5.3 7.7 0.35 0.34 0.77 3.43 0.17 34.1 1.12 0.2 SLE-05 400 69 5.9 7.6 0.39 0.43 1.36 4.34 0.29 31.72 1.25 0.19 SLE-06 500 95 7.5 7.5 0.33 0.22 0.39 2.42 0.12 36.22 0.58 0.09 R1 50 88 9.9 10 0.38 0.16 0.23 0.54 0.06 38.37 0.27 0.21 R2 300 91 10.2 10.3 0.44 <0.01 0.03 <0.001 0.01 42.9 0.11 0.26 Fig. 3. (a, b) View of eolianite on Pliocene clays, (c, d) SEM and thin section images of eolianite samples, respectively, (e) rhizolith within the eolianite, (f) inner (white star), middle (gray star) and outer (black star) rings.
A.E. Erginal et al. / Quaternary International 296 (2013) 168e175 172
coastal dunes prior to cementation. The abrupt decrease in resis-tivity values at the most landward extension of the survey lines points to the boundary of the eolianite being at 100 me105 m backshore.
3.2. OSL ages and implications for Late Pleistocene sea-levels Optical luminescence (accurate to within approx. 5e10%) ascertains the depositional age of the quartz grains within the
Fig. 5. (a, b, c) Inverse model resistivity sections of ERT1, ERT2 and ERT3 lines, respectively. Fig. 4. (a, b, c) Measured apparent resistivity pseudosections of ERT1, ERT2 and ERT3 lines, respectively.
eolianite. The oldest OSL age (SLE-06) obtained from the sample overlying the Pliocene clays at 5 m below the rock surface was dated at 138.0 13.6 ka (Table 1). Based on marine isotope stage (MIS) records (Chappell and Shackleton, 1986), these ages suggest that dune sands were deposited during the early phase of the marine isotope stage 5e period (MIS 5e) or transition stage from MIS 6 to MIS 5e, when accuracy values are considered. Considering sea-level changes occurring in the Black Sea before and during deposition of eolianite components, available data has attested an increasing trend in the Black Sea’s hydrologic budget during the Karangatian transgression, coinciding with so-called Eemian (Mikulinian) interglacial which spanned 125 ka to 65 ka (Panin and Popescu, 2007), during which the sea-level was 6e8 m higher than the present (Federov, 1978;Chepalyga, 1984;Svitoch et al., 2000). This highstand, allowing a connection with the Mediterranean via the Bosphorus and Dardanelles, could be of great importance for the production of connective calcium carbonate cement in shallow shelf plains. It is well-known that numerous carbonate-laden deposits accumulated during interglacial highstands on the coastal shelf and are the main source for reworking by offshore winds leeward (Abegg et al., 2001;Brooke, 2001), allowing, in turn, initial cementation of dune sands, resulting in eolianites. Consid-ering highstand sea-level conditions prior to deposition, the detected connective calcite and aragonite, abundant ooids within the eolianite, and root casts reveal the wind-blown drifting of carbonate from subtidal to supratidal. Similar eolianites as high-stand cemented dunes have been recorded in the Bahamas (Hearty and Kindler, 1995; Kindler and Hearty, 1995), southeastern Australia (Murray-Wallace et al., 2001), Lord Howe Island, Tasman Sea (Woodroffe et al., 1995) and the western Mediterranean (Fumanal, 1995).
4. Conclusion
Thefirst record of eolianite on the Black Sea coast of Turkey was discussed in the light of its main visible characteristics, internal structure and depositional optical ages. The main diagnostic facies characteristics of these carbonate dunes at outcrop and microscopic scale are (1) the existence of high angle landward-dipping planar foresets, (2) abundant CaCO3 as connective cement material, (3)
fine-grained and well-sorted sand content, and (4) ooids and fossil root casts or rhizoliths as organosedimentary components. OSL dating using SAR was applied to quartz minerals dominating within the eolianite. Quartz from eolianite samples was bright in lumi-nescence, and sensitivity changes were corrected successfully using the response to a test dose. The OSL ages, which appear reliable based on growth curves and dose recovery tests, showed that the onset of dune sand accumulation on Pliocene sandy clays took place at 138 ka over the underlying Pliocene unit. This early phase of dune sand accumulation is defined by sharp irregular contact with the underlying older unit, which pinpoints a rugged topography fossilized by eolian sands. It may also be concluded that a combined use of eolian facies patterns with electrical resistivity imaging provides useful insights for the assessment of such relict coastal landforms.
Acknowledgements
We thank Dr. Aydın Büyüksaraç for his suggestion to use resis-tivity data in the research. We are also grateful to Dr. Mustafa Karabıyıkoglu and Dr. Mustafa Bozcu for their helpful suggestions. Graham Lee is thanked for putting effort into linguistic corrections of the early version of this paper. This study was funded by the
Research Foundation of Çanakkale Onsekiz Mart University (Project Number: 2011/41).
References
Abdüsselamoglu, S¸., 1963. Geology of Kocaeli Peninsula. Mineral Research and Exploration of Turkey, Unpublished Report No 3249, Ankara.
Abegg, F.E., Loope, D., Harris, P.M., 2001. Carbonate eolianites: depositional models and diagenesis. In: Abegg, F.E., Harris, P.M., Loope, D.B. (Eds.), Modern and Ancient Carbonate Eolianites: Sedimentology, Sequence Stratigraphy, and Diagenesis. SEPM Special Publication 71, pp. 17e30.
Adamiec, G., Aitken, M., 1998. Dose-rate conversion factors: update. Ancient TL 16, 37e49.
Alonso-Zarza, A.M., Genise, J.F., Cabrera, M.C., Mangas, J., Martín-Pérez, A., Valdeolmillos, A., Dorado-Valiño, M., 2008. Megarhizoliths in Pleistocene aeolian deposits from Gran Canaria (Spain): ichnological and palaeoenvironmental significance. Palaeogeography Palaeoclimatology Palaeoecology 265, 39e51. Bardaji, T., Goy, J.L., Zazo, C., Hillaire-Marcel, C., Dabrio, C.J., Cabero, A., Ghaleb, B.,
Silva, P.G., Lario, J., 2009. Sea level and climate changes during OIS 5e in the Western Mediterranean. Geomorphology 104, 22e37.
Bøtter-Jensen, L., 1997. Luminescence techniques: instrumentation and methods. Radiation Measurements 17, 749e768.
Brooke, B., 2001. The distribution of carbonate eolianite. Earth-Science Reviews 55, 135e164.
Chappell, J., Shackleton, N.J., 1986. Oxygen isotopes and sea level. Nature 324, 137e140.
Chepalyga, A.L., 1984. Inland sea basins. In: Velichko, A.A., Wright, H.E.J., Barnowsky, C.W. (Eds.), Late Quaternary Environments of the Soviet Union, English Edition. University of Minnesota Press, Minneapolis, pp. 229e247. Cohen, A.S., 1982. Paleoenvironments of root casts from the Koobi Fora Formation,
Kenya. Journal of Sedimentary Petrology 52, 401e414.
Defant, A., 1961. Physical Oceanography, vol. 2. Pergamon, Oxford, 404e407 pp. Dunham, R.J., 1962. Classification of carbonate rocks according to depositional
texture. In: Ham, W.E. (Ed.), Classification of Carbonate Rocks. American Asso-ciation of Petroleum Geologists Memoir 1, pp. 108e121.
Erginal, A.E., Ekinci, Y.L., Demirci, A., Avcıoglu, M., Öztürk, M.Z., Türkes¸, M., Yigitbas¸, E., Depositional characteristics of carbonate-cemented fossil eolian sand dunes: Bozcaada Island, Turkey. Journal of Coastal Research,in press.
Ertek, T.A., 1995. Results of Geomorphological Researches in Northeastern Part of Kocaeli Peninsula, NW Anatolia (Turkey). In: Review of Istanbul University 2, 41e46 pp.
Fairbridge, R.W., Johnson, D.L., 1978. Eolianite. In: Fairbridge, R.W., Bourgeois, J. (Eds.), The Encyclopedia of Sedimentology. Dowden, Hutchinson and Ross, Stroudsburg, PA, pp. 279e282.
Federov, P.V., 1978. Pleistotsen Ponto-Kaspiia (The Pleistocene of the Ponto-Caspian Region). Trudy Geologicheskogo Instituta Akademii Nauk SSSR, Nauka, Moscow, 168 p.
Frébourg, G., Hasler, C.-A., Guern, P.L., Davaud, E., 2008. Facies characteristics and diversity in carbonate eolianites. Facies 54 (2), 175e191.
Fumanal, M.P., 1995. Pleistocene dune systems in the Valencian Betic cliffs (Spain). INQUA Subcommission on Mediterranean and Black Sea Shorelines. Newsletter 17, 32e38.
Hearty, P.J., Kindler, P., 1995. Sea-level highstand chronology from stable carbonate platforms (Bermuda and the Bahamas). Journal of Coastal Research 11, 675e689.
Kelletat, D., 1991. Geomorphological aspects of eolianites in Western Australia. In: Bruckner, H., Radtke, U. (Eds.), Von der Nordsee bis zum Inischen Ozsean. Franz Steiner Verlag, Stuttgart, pp. 181e198.
Kindler, P., Hearty, P.J., 1995. Pre-Sangamonian eolianites in the Bahamas? New evidence from Eleuthera Island. Marine Geology 127, 73e86.
Kiyak, N.G., Erginal, A.E., 2010. Optical stimulated luminescence dating study of eolianite on the Island of Bozcaada, Turkey: preliminary results. Journal of Coastal Research 26, 673e680.
Klappa, C.F., 1980. Rhizoliths in terrestrial carbonates: classification, recognition, genesis, and significance. Sedimentology 26, 613e629.
Kraus, M.J., Hasiotis, S.T., 2006. Significance of different modes of rhizolith preser-vation to interpreting paleoenvironmental and paleohydrologic settings: examples from paleogene paleosols, Bighorn basin, Wyoming, U.S.A. Journal of Sedimentary Research 76, 633e646.
Loreau, J.P., Purser, B.H., 1973. Distribution and ultrastructure of Holocene ooids in the Persian Gulf. In: Purser, B.H. (Ed.), The Persian Gulf. Springer-Verlag, New York, pp. 279e328.
Loke, M.H., Barker, R.D., 1996. Rapid least-squares inversion of apparent resistivity pseudosections by a quasi-Newton method. Geophysical Prospecting 44, 131e152.
Loke, M.H., Acworth, I., Dahlin, T., 2003. A comparison of smooth and blocky inversion methods in 2D electrical resistivity imaging. Exploration Geophysics 34, 182e187.
Murray, A.S., Mejdahl, V., 1999. Comparison of regenerative-dose single-aliquot and multiple-aliquot (SARA) protocols using heated quartz from archaeological sites. Quaternary Science Reviews (Quaternary Geochronology) 18, 223e229. Murray, A.S., Wintle, A.G., 2000. Luminescence dating of quartz using an improved
single-aliquot regenerative-dose protocol. Radiation Measurements 32, 57e73. A.E. Erginal et al. / Quaternary International 296 (2013) 168e175
Murray-Wallace, C.V., Brooke, B.P., Cann, J.H., Belperio, A.P., Bourman, R.P., 2001. Whole rock aminostratigraphy of the Coorong Coastal Plain, South Australia: towards a 1 million year record of sea-level highstands. Journal of the Geological Society of London 158, 111e124.
Nathan, R.P., Mauz, B., 2008. On the dose rate estimate of carbonate-rich sediments for trapped charge dating. Radiation Measurements 43, 14e25.
Okay, A.C., 1948. Geologische Untersuchung des Gebietes zwischen S¸ile, Mudarlı, Kartal und Riva in Kocaeli, Bityhnien, Türkei. In: Istanbul University Review of Faculty of Science (Serial B) 13, 311e335 pp.
Olayinka, A.I., Yaramancı, U., 2000. Assessment of the reliability of 2D inversion of apparent resistivity data. Geophysical Prospecting 48, 293e316.
Panin, N., Popescu, I., 2007. The Northwestern Black Sea: climatic and sea-level changes in the late Quaternary. In: Yanko-Homback, V., Gilbert, A.S., Panin, N., Dolukhanov, P.M. (Eds.), The Black Sea Flood Question. Changes in Coastline, Climate and Human Settlement, pp. 387e404.
Qi, L., Carr, T.L., 2006. Neural network prediction of carbonate lithofacies from well logs, Big Bow and Sand Arroyo Creekfields, Southwest Kansas. Computers & Geosciences 32, 947e964.
Schlicting, E., Blume, E., 1966. Bodenkundliches Practicum. Verlag paul Parey, Hamburg un Berlin.
Svitoch, A.A., Selivanov, A.O., Yanina, T.A., 2000. Paleohydrology of the Black Sea Pleistocene basins. Water Resources 27 (6), 594e603.
Woodroffe, C.D., Murray-Wallace, C.V., Bryant, E.A., Brooke, B., Heijnis, H., Price, D.M., 1995. Late Quaternary sea-level highstands in the Tasman Sea: evidence from Lord Howe Island. Marine Geology 125, 61e72.
Yılmaz, Y., Gökas¸an, E., Erbay, A.E., 2010. Morphotectonic development of Marmara Region. Tectonophysics 488, 51e70.
Yigitbas¸, E., Elmas, A., Sefunç, A., Özer, N., 2004. Major neotectonic features of eastern Marmara region, Turkey: development of the Adapazarı-Kar-asu corridor and its tectonic significance. Geological Journal 39, 179e198.
