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Journal of Coastal Research 26 2 350358 West Palm Beach, Florida March 2010
Investigation of Beachrock Using Microanalyses and OSLDating: A Case Study from Bozcaada Island, Turkey
Ahmet Evren Erginal, Nafiye Gunec Kyak, and Beyhan Ozturk
Department of GeographyFaculty of Sciences and Arts
Canakkale Onsekiz Mart University
Canakkale, Turkey
Department of PhysicsFaculty of Sciences and Arts
Isk University
Istanbul, Turkey
ABSTRACT
ERGINAL, A.E.; KIYAK, N.G., and OZTURK, B., 2010. Investigation of beachrock using microanalyses and OSLdating: a case study from Bozcaada Island, Turkey. Journal of Coastal Research, 26(2), 350358. West Palm Beach(Florida), ISSN 0749-0208.
We investigated the origin and absolute age of beachrock samples on Bozcaada Island, located on the northern AegeanSea coast of Turkey, using energy dispersive X-ray spectroscopy (EDX) and scanning electron microscopy (SEM)analyses and optically stimulated luminescence (OSL) dating. Various types of cements were identified, such as mi-critic, meniscus, and biologic cements, revealing that the beachrock could have occurred as a result of the combinedeffects of marine-phreatic and supratidal cementation conditions. Optical dating results showed that the formation ofbeachrock ranged in age from 5.41 0.58 ka BP to 0.33 0.05 ka BP. However, much of the beachrock body (about3 m in thickness) is drowned or submerged today, suggesting that submerged beachrocks extending to 5 m date toearlier times than the start of the cementation period discussed herein.
ADDITIONAL INDEX WORDS: Beachrock, intertidal lithification, luminescence dating, Bozcaada Island, Turkey.
INTRODUCTION
Beachrock is a carbonate-cemented sedimentary rock dip-
ping gently toward the sea. Even though this occurrence has
been reported from various climatic regions (Alexanderson,
1972; Beier, 1985; Friedman and Gavish, 1971; Holail and
Rashed, 1992; Kneale and Viles, 2000; Moore, 1973; Sellwood,
1995; Taylor and Illing, 1969; Webb, Jell, and Baker, 1999),
intertidal environments of tropical and subtropical beacheshave the most favorable conditions for the occurrence of these
formations (Bricker, 1971; Ginsburg, 1953; Neumeier, 1998).
Cementation of loose beach materials that results in the for-
mation of beachrock is controlled by a variety of factors. In
this respect, the physicochemical attributes of seawater and
underground waters coming from the land is of significance.
In addition, the chemical composition and crystal micromor-
phology of connective cement materials give practical clues
that shed light on both the origin and place of beachrock for-
mation. With regard to the cementation environment and fac-
tors governing the precipitation of calcium carbonate cement,
different possible causes have been discussed, such as mixing
of marine and meteoric waters (Moore, 1973; Schmalz, 1971),
CO2 degassing from shallow groundwaters (Hanor, 1978),evaporation of seawater (Meyers, 1987; Moore and Billings,
1971; Scoffin, 1970; Stoddart and Cann, 1965; Taylor and Ill-
ing, 1969), and biological impacts (Krumbein, 1979; Neu-
meier, 1999; Webb, Jell, and Baker, 1999).
Even though first definitions date back to the early 1800s
on the southern Anatolian coastline of Turkey (Spratt and
DOI: 10.2112/08-1151.1 received 31 October 2008; accepted in revi-sion 24 November 20 08.
Forbes, 1847), the occurrence of beachrock throughout Tur-
keys long (8333 km) coastline is little known with the excep-
tion of a few studies. In previous publications, these occur-
rences have been recognized in the Saros Gulf and the Med-
iterranean Sea coastline of Turkey (Avsarcan, 1997; Bener,
1974; Bodur and Ergin, 1992; Erginal et al., 2008; Erol, 1972;
Ertek and Erginal, 2003; Kelletat, 2006). The present paper
discusses, for the first time, cementation history and absolute
age of beachrock on the south coast of Bozcaada Island in
northwest Turkey by taking into account cementation pat-
terns within beachrock cements based on microanalytical
techniques. On the studied beach, beachrocks are only ex-
posed on the south coast of the island. We studied this beach-
rock because of its unexpected thickness (3.50 m) in this mi-
crotidal environment with, at present, a tide range between
20 and 40 cm. Several microanalyses and luminescence dat-
ing studies were carried out.
Study Area
The Island of Bozcaada, with a coastline of 36.41 km and
a total area of 37.51 km2, is located 4 km west of the Biga
Peninsula in the northwest Anatolian part of Turkey (Figure1). The island is a westward continuation of this peninsula,
evidenced by its very similar geologic and geomorphologic
characteristics. According to the existing geologic literature
(Erguvanl, 1955; Kalafatcoglu, 1963; Saltk and Saka,
1972), the geology of the island is made up of several rock
units that range in age from Palaeozoic to Holocene. Palaeo-
zoic metamorphic rocks consisting of marble and schist and
underlying serpentine form the visible basement and crop out
only on the southwest part of the island. These old units,
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351Beachrock on the Bozcaada Island, Turkey
Journal of Coastal Research, Vol. 26, No. 2, 2010
Figure 1. Map showing location of studied beachrock and sampling sites.
extending in a NW-SE direction, have dips varying between
35 and 40 toward the southeast and are overlain uncon-
formably by conglomerate, limestone, and flysch of Eoceneage. The Upper Mioceneaged conglomerate, sandstone, clay-
stone, limestone, and andesite, however, dominate the geol-
ogy of the island. The western part of the island is formed of
coastal dune sands.
According to the climatic data recorded at Bozcaada me-
teorological station (3950 N and 2604 E, 28 m above sea
level) for the period between 1975 and 2003, the area receives
annual average precipitation of 462.5 mm. Maximum and
minimum precipitations occur in winter (89.4 mm in Decem-
ber) and summer (5.5 mm in August). The average temper-
ature is 15.4C. The coldest and the warmest months are Feb-
ruary (8.3C) and July (23C). The island is one of the wind-iest areas of the country. Prevailing winds come from the
northeast. The number of stormy and strongly windy days is
86.5 and 156.5, respectively.
MATERIALS AND METHODS
Microanalyses of Beachrock Cement
Beachrock samples along one transect from underwater
beds to upper-intertidal exposures were collected for micro-
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352 Erginal, Kyak, and Ozturk
Journal of Coastal Research, Vol. 26, No. 2, 2010
Table 1. Generalized single-aliquot regeneration (SAR) sequence.
Run 1: Regenerative dose, Di
(i 1, natural dose; i 2, 3, 4, 5, 6, generative
doses)
Run 2: Preheat (260C for 10 s)
Run 3: OSL for 40 s at 125C, LiRun 4: Test dose, T
d
Run 5: Heat to 180C, TL
Run 6: OSL for 40 s at 125C, Ti
Repeat Run 1
Figure 2. Growth curves using the corrected OSL dose points from a
representative sample BYT-4 are shown; all dose points correspond to a
linear function.
analyses (Figure 1). The elemental composition and micro-
morphology of beachrock cements was examined using ener-
gy dispersive X-ray spectroscopy (EDX) with a Bruker AXS
XFlash (Madison, Wisconsin) and scanning electron micros-
copy (SEM) with a Zeiss EVO 50 EP (Jena, Germany).
Sample Preparation and Optically StimulatedLuminescence Measurements
Seven beachrock samples from Bozcaada Island were dated
using optically stimulated luminescence (OSL). The outer
surface of about 5 mm was removed first from all samplesand inner parts were crushed in a mortar. Quartz grains of
90180 m were extracted with usual chemical procedures
described in detail by Erginal et al. (2008).
An automated Ris TL/OSL-DA-15 reader (Roskilde, Den-
mark) equipped with an internal 90Sr/90Y beta source (0.1
Gy s1) was used for all OSL measurements (Btter-Jensen
et al., 2000). Blue light emitting diodes, or LEDs (470 nm,
40 mW cm2) and infrared LEDs (880 nm, 135 mW cm2)
were used for stimulations where infrared stimulation was
employed to check the detection of feldspar contamination.
Luminescence signal detection was made using an EMI
9635QA photomultiplier tube (ET Enterprises Limited, UK),
fitted with Hoya U-340 filters (Hoya Corporation, USA) of 7.5
mm total thickness.
The dose rate assessment was based on gamma spectros-
copy recorded in situ. The total dose rate required for OSL
age was estimated from the gamma dose rate measured in
situ and from the spectral data using conversion factors pre-
sented by Olley, Murray, and Roberts (1996).
Growth Curves and Equivalent Dose Estimate
Optically stimulated luminescence dating techniques have
been widely used to estimate the radiation dose (equivalent
or paleodose) accumulated in quartz extracted from sediment
materials (Aitken, Smith, and Rhodes, 1989). The technique
is based on the comparison of the natural OSL signal with
the OSL signals produced by known laboratory doses. Thesingle-aliquot regenerative-dose protocol (OSL-SAR) used
here (Table 1) employs a cycle of measurements in which the
natural OSL is first measured (Mejdahl and Btter-Jensen,
1994; Murray and Roberts, 1998; Murray and Wintle, 2000).
The samples were divided into subsamples (aliquots) and
each aliquot was stimulated for 40 s. The temperature de-
pendence of OSL intensity and possible effect on the dose for
each sample was examined for the temperature range be-
tween 200260C (preheat plateau), and a preheat tempera-
ture of 260C was selected for further OSL measurements of
the SAR sequence presented in Table 1. The SAR sequence
has six cycles: in the first cycle (i 1), the natural OSL was
measured; the following three cycles (i 2, 3, 4) are regen-
erative OSL doses; the fifth cycle (i 5) is a zero dose or
bleach; in the final cycle (i 6), the first generative dose was
measured again to check the repeatability of measurements.
In each cycle, aliquots were preheated at 260C for 10 s prior
to all natural and regenerative OSL measurements (Li) to
remove unstable signals from the OSL curves. A test dose of
about 1020% of the expected natural dose was given to each
sample to monitor the sensitivity change between the cycles.
Then the test dose OSL signal (Ti) was measured following acut-heat temperature of 180C. All OSL signals were correct-
ed using the test dose OSL response to the corresponding
OSL signal (Li/Ti); they were then used to construct a dose
response curve. The dose response curve from a representa-
tive sample, BYT-4, covering regenerative dose points from 0
to 21 Gy, can be fitted with a linear function as seen in Figure
2. The natural dose De is obtained from the interpolation of
corrected natural signals (Ln/Tn) on the dose-response curve.
For the reliability of OSL measurements, the fifth regen-
eration dose (R5) was administered to the same aliquot equal
to the first regeneration dose (R1) to check the repeatability
of a regenerative dose on the dose-response curve. Namely,
the recycling ratio (R5/R1) of a dose point on the curve is ex-
pected to be close to unity for reliability (Murray and Wintle,2000). The recycling ratios for the samples measured in this
study were generally close to unity, except for a few aliquots
that were not taken into account for age estimation.
RESULTS AND DISCUSSION
Composition and Micromorphology of Cements
The studied beachrock beds are backed by a gently sea-
wardinclined (510) sandy beach with a 10 m width strike
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353Beachrock on the Bozcaada Island, Turkey
Journal of Coastal Research, Vol. 26, No. 2, 2010
Figure 3. Views of exposed beachrocks: (a) beds with gentle dips toward the sea, (b) underwater beachrock fragments, and (c) beachrock beds followed
up to 15 m offshore terminating at 4 m depth.
NW-SE, roughly parallel to that of the general trend of the
present shoreline. It is an indurated sedimentary formation
80 m in length, 22 m in width, and 3.5 m thick, with litho-
logically identical petrographic composition to that of the ad-
jacent sandy beach. In fact, both adjoining beach and beach-
rocks are composed of coarse sand and small gravels of sand-
stone, basalt, limestone, and andesite. In the vertical section,
the sequence is made up of alternating layers of sand and
moderate to well-rounded gravels derived from the above-mentioned rocks. Quartz, plagioclase, and mica fragments
form the main mineral component. The alternating beds vary
in thickness from a few cm to 20 cm and have dips sloping
seaward at angles ranging between 4 and 16 (average 10;
see Figure 3a). The exposed beachrock reaches up to 0.75 m
above sea level.
From the morphological point of view, the beachrock out-
crops appear to begin in a cape composed of Miocene lime-
stone with mactra fossils in the northwest and extend dis-
continuously toward the southwest for a distance of 7080 m
(Figures 1 and 3b). It is surprising that this platform shows
an abrupt termination in the middle of the sheltered bay
where it occurs. Underwater observations carried out to a 5
m depth also showed the absence of beachrock blocks in this
part. Field observations show that beachrock beds are char-
acterized by irregular or pitted surfaces. The uppermost sur-
faces, particularly corrosion pits having sizes up to 1 m in
width, are either colonized by marine algae or occupied bysea salt accumulations. The beds, being in touch with the
shoreline, are also inhabited by rock barnacles such as Bal-
anus and Patella species. Due to marine erosion along struc-
tural weaknesses such as closely spaced orthogonal joints and
bedding planes, which allow the easy penetration of seawa-
ter, the beachrocks comprise several angular blocks. At their
most seaward extent, beachrocks are followed up to 15 m off-
shore and terminate at a 4 m depth (Figure 3c). Under-
water observations demonstrated that submerged beachrock
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354 Erginal, Kyak, and Ozturk
Journal of Coastal Research, Vol. 26, No. 2, 2010
ledges are widely broken into orthogonal blocks along dense
joints. The petrographic composition of beachrock beds is
identical to those of the exposed ones.
Samples extracted from various levels of the exposed
beachrock ledges showed mainly the micromorphologic char-
acteristics of beachrock cement. The EDX data obtained from
the cement material and cement-grain boundaries within the
beachrocks reveal the abundant presence of wollastonite(CaSiO3), albite, ortoclase, and quartz minerals, as well as
various elements such as C, Mg, Al, Si, Cl, Ca, Fe, O, K, Na,
and S.
Micritic Cements
In many samples, the cement material begins with the
widespread occurrence of micritic coatings over the tops and
flanks of the amalgamated grains. The EDX data showed
that the cement is composed of high Mg-calcite. Albite,
quartz, and potassium feldspars forms common mineral con-
stituents. The coatings composed of microcrystalline calcite
crystals that range in thickness from a few m to 10 m form
the initial stage of cement precipitation (Scoffin, 1987). Mi-critic (12 m thick) envelopes are followed by acicular crys-
tals with lengths ranging between 20 and 60 m and diam-
eters between 5 and 10 m (Figures 4a and b). The crystal
morphology of these cements fixes well with that of aragonite
(Gischler and Lomando, 1997; Tucker and Wright, 1990).
These equigranular monocrystals stand perpendicular to
grain surfaces and possibly form the second generation of the
cementation process, and they are indicative of precipitation
from seawater (Neumeier, 1998; Stoddart and Cann, 1965;
Taylor and Illing, 1969).
Some samples are dominated by micritic overgrowths on
siliciclasts (Figures 4c and d) consisting of considerably high-
er amounts of Na (6.88%), Mg (3.37%), Si (27.24%), Cl
(7.23%), Ca (11.02%), Fe (3.28%), and O (40.98%) in compar-
ison to those of the averages of the other samples. Albite,
quartz, and wollastonite were defined as dominant compo-
nents. Well-rounded siliciclasts with a diameter up to 500 m
and mineral fragments are amalgamated to each other with
thick (approximately 40 m) micritic crystals (510 m). Al-
though voids are common with sizes between 20 and 150 m,
this cement has a very tight appearance owing to the well-
developed overgrowths of intricate micrite crystals that pro-
trude from 1020-m-thick cryptocrystalline micrite coating
the grain surfaces. These forms, together with EDX data, in-
dicate direct but possibly more rapid precipitation from the
evaporation of seawater. The presence of micritization ap-
proximately 30 m in thickness and dominated by the pres-ence of micrite coatings, cryptocrystalline pore fillings, and
bladed calcite crystals was observed on the mineral frag-
ments composed of quartz and potassium feldspar (ortoclase).
Such cements comprise C (14.93%), Na (1.43%), Mg (1.32%),
Al (0.62%), Si (10.83%), Cl (1.15%), K (0.34%), Ca (10.14%),
Fe (0.85%), and O (58.39%). Within some voids, filaments of
marine algae are also present together with newly formed
calcite accumulations and aragonite needles (Figures 4e and
f).
Meniscus Cement
Scanning electron microscope images taken from one sam-
ple demonstrated the exclusive presence of meniscus cement
that amalgamates well-rounded siliciclastic grains (Figures
4g and h). The thickness of the bridge ranges between 50 and
100 m. The cement is a mixture of C (14.56%), Mg (0.67%),
Si (18.33%), Cl (0.52%), Ca (1.88%), Fe (0.76%), and O
(62.40%). Quartz grains with an angular shape range in sizefrom 10 m to 50 m. Both EDX data and textural charac-
teristics refer to carbonate-rich meteoric conditions in terms
of a diagenetic environment (Folk, 1974; Friedman, 1964;
Scoffin and Stoddart, 1983; Spurgeon, Davis, and Shinnu,
2003). Such cements usually precipitate from the mixing of
marine and meteoric waters (Moore 1973; Rey et al., 2004;
Schmalz, 1971).
Biologic Cements
At their most leeward extent, beachrocks showed explicit
marks of biological control on cementation in the upper in-
tertidal zone (Figures 5a and b). The upper surface of the
beachrock is colonized by marine algae and has a floppy andbrittle structure with large voids exceeding 100 m in some
places. The cemented materials are composed of angular to
poorly rounded siliciclasts with fungal filaments. The cement
contains average amounts of C (16.33%), Na (0.93%), Mg
(1.32%), Al (1.19%), Si (3.74%), Cl (1.12%), Ca (16.46%), Fe
(2.35%), and O (56.46%). Both fungal filaments and mineral
surfaces appear to be covered with small carbonate nodules,
the precipitation of which is also confirmed by an increase in
the total amount of Ca. These forms reveal that beachrock
cementation was also associated with precipitation of biolog-
ically produced cement materials under marine-phreatic con-
ditions, as suggested previously by several authors (Jones
and Kahle, 1993; Khadkikar and Rajshekkar, 2003; Verrec-
chia and Verrecchia, 1994; Webb, Jell, and Baker, 1999).
The Age of Beachrock: Implications for Variations inSea-Level and Tidal Range
The gamma dose rates were measured in situ, and the beta
dose rates were obtained from concentrations of the major
radioactive isotopes of the uranium and thorium series and
of potassium (Olley, Murray, and Roberts, 1996). The cosmic
ray contribution was estimated using altitude, latitude, and
depth from the surface (Prescott and Hutton, 1994). The buri-
al dose rates ranged from 1.37 0.03 to 1.57 0.03 mGy/a.
The results of radiometric analysis and dose values obtained
are summarized in Table 2 with error due to statistical fluc-
tuations in counting. The OSL ages of the samples taken fromdifferent profiles are presented in Table 2 together with the
number of aliquots evaluated for each sample. The optical
luminescence ages from each sample were found to be be-
tween about 300 years to 5.41 ka, and repeated measure-
ments were in good agreement with other reported beach-
rocks around the world (Vousdoukas, Velegrakis, and Plo-
maritis, 2007).
As presented in Table 2, the dated beachrocks yielded var-
ious ages from 5.41 0.58 ka to 0.33 0.05 ka, suggesting
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355Beachrock on the Bozcaada Island, Turkey
Journal of Coastal Research, Vol. 26, No. 2, 2010
Figure 4. SEM images of the beachrock samples: (a, b) Micritic coatings followed by acicular aragonite needles; (c) meniscus cement growing on micritic
coatings; (d) detail of meniscus cement marked in square (c); (e, f) cryptocrystalline micritic coatings followed by intricate micrite overgrowths; (g, h)
micrite coatings, cryptocrystalline pore fillings, and bladed calcite crystals. Note the presence of algae filaments, aragonite needles, and calcite accumu-
lations shown in square (h).
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356 Erginal, Kyak, and Ozturk
Journal of Coastal Research, Vol. 26, No. 2, 2010
Figure 5. (a and b) SEM images showing biologic control on cementation in the upper intertidal zone of (submerged) beachrock. (b) is closer view of the
surfaces of grains with dense algae filaments and carbonate precipitates.
Table 2. The OSL-SAR ages and equivalent dose obtained for samples
taken from different profiles of the beachrock, and the dose rate of environ-
ment.
Sample
Lab Code
Depth
(cm)
Age
(ka)
SAR
De
(Gy) n
Dose Rate
(Gy/ka)
BYT-01 50 0.33 0.05 0.51 0.07 12 1.54 0.03BYT-02 35 0.63 0.07 0.86 0.09 12 1.37 0.03
BYT-03 25 0.84 0.13 1.32 0.20 12 1.57 0.03BYT-04 35 1.02 0.13 1.40 0.18 12 1.37 0.03BYT-05 30 3.65 0.82 5.70 1.28 12 1.56 0.03
BYT-06 20 5.41 0.58 8.73 0.92 10 1.61 0.03
n the number of aliquots.
episodically developed cementation over the last 5 ka. How-
ever, these ages are, from bottom to top in the vertical sec-
tion, representative for the exposed beachrock with a 75 cm
thickness. The time interval between the ages obtained would
be related to destruction caused by marine erosion, intertidal
weathering, and subsequent removal of various strata (Fig-
ures 3a and b). Such erosive stages would be favored during
small-scale sea-level fluctuations impeding complete cemen-
tation of beach sediments.Another contradiction results from the abnormal thickness
(3.5 m) of the beachrock studied, considering the average val-
ue (0.20 m in normal conditions) of the tidal range for the
eastern Mediterranean coastline (Kelletat, 2006). A differ-
ence of more than 3 m between the present tidal range and
the thickness of the beachrock is a sporadic condition that
some beachrock researchers encounter elsewhere (Amieux et
al., 1989; Kelletat, 2006; Mabesoon, 1964; Vieira and De Ros,
2007). According to Kelletat (2006), Only a supratidal situ-
ation during cementation can explain the great thickness and
horizontal extension of beachrocks on the majority of coast-
lines of the world. Considering this assumption, favorable
conditions for supratidal cementation in the study area might
have occurred when the sea level was at 2 m 3500 years
ago BP (Kayan, 1994). On the basis of 14C dating of marine
mollusks, obtained by drilling from the Karamenderes flood-
delta plain 4 km west of Bozcaada Island, the sea-level rise
slowed and stopped about 6000 BP and reached a level sim-
ilar to that of the present (Kayan, 1999). This period can beconsidered suitable for intertidal cementation of the oldest-
dated (5.41 0.58 ka) beachrock in the studied beach. The
following stagea sea-level fall of 2 moccurred between
5000 and 3500 BP (Kayan, 1995); this is the most significant
sea-level fluctuation in the last 5000 years, and it caused a
large beach zone to emerge, providing more sediment and
more carbonate for the occurrence of cementation. Thus we
consider the samples of beachrock dated to 3.65 0.82 ka to
likely correspond to the period of sea-level fall; this is con-
firmed by the widespread presence of meniscus cement fa-
vored by meteoric waters, supporting the contention of Kel-
letat (2006). The other beachrocks are, however, composed
entirely of cements that evolved under marine-phreatic con-
ditions, when the sea level was not more than 40 cm lowerthan the present level (Figure 6).
CONCLUSIONS
Our data, based on cementation patterns, optical lumines-
cence dating, and field data, reveal that intertidal and su-
pratidal conditions may collectively influence the formation
of beachrock. With the exception of samples dated to 3.65
0.82 ka that are dominated by the presence of meniscus ce-
ment, many samples were characterized by the predominance
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357Beachrock on the Bozcaada Island, Turkey
Journal of Coastal Research, Vol. 26, No. 2, 2010
Figure 6. Positions of the OSL ages of beachrock samples on the sea-
level curve, prepared by Kayan (1999).
of marine-phreatic cements. Beachrocks ranged in age from
0.33 0.05 ka BP to 5.41 0.58 ka BP. The fact that much
of the beachrock body (about 3 m in thickness) appears to be
drowned or submerged today is likely associated with a sea-
level rise in the last 3 ka. These submerged beachrocks ex-
tending to 5 m would have older ages. Further study is
needed for better understanding of the nature and age ofbeachrock cementation in this coastal area.
ACKNOWLEDGMENTS
This paper was supported financially the by Research
Foundation of Canakkale Onsekiz Mart University (Project
Number 2008/32).
LITERATURE CITED
Aitken, M.J.; Smith, B.W., and Rhodes, E.J., 1989. Optical dating:recapitulation on recuperation. In: Long and Short Range Limitson Luminescence Dating (Oxford, United Kingdom), OccasionalPublication No. 9, Research Laboratory for Archaeology and theHistory of Art, pp. 510.
Alexanderson, T., 1972. Mediterranean beachrock cementation: ma-rine precipitation of Mg-calcite. In: Stanley, D.J. (ed.), The Medi-terranean Sea: A Natural Sedimentation Laboratory. New York:Dowden, Hutchinson and Ross, pp. 203223.
Amieux, P.; Bernier, P.; Dalongeville, R., and de Medwecki, V., 1989.Cathodoluminescence of carbonate-cemented Holocene beachrockfrom the Togo coastline (West Africa): an approach to early dia-genesis. Sedimentary Geology, 65, 261272.
Avsarcan, B., 1997. Theories on beachrock formation and some char-acteristics of beachrocks on Turkeys coasts. Geographical Journalof Istanbul University, 5, 259282.
Beier, J.A., 1985. Diagenesis of Quaternary Bahamian beachrock:petrographic and isotopic evidence. Journal of Sedimentary Pe-trology, 55, 755761.
Bener, M., 1974. Beachrock Formation on the Coastal Part of An-talya-Gazipasa. Istanbul: Istanbul University Institute of Geog-raphy Publications, 75.
Bodur, M.N. and Ergin, M., 1992. Holocene sedimentation patternsand bedforms in the wave- current-dominated nearshore waters ofeastern Mersin Bay (eastern Mediterranean). Marine Geology,108, 7393.
Btter-Jensen, L.; Bulur, E.; Duller, G.A.T., and Murray, A.S., 2000.Advances in luminescence instrument systems. Radiation Mea-surements, 32, 523528.
Bricker, O.P., 1971. Introduction: beachrock and intertidal cement.In: Bricker, O.P. (ed.), Carbonate Cements. Baltimore, Maryland:John Hopkins Press, pp. 13.
Erginal, A.E.; Kyak, N.G.; Bozcu, M.; Ertek, T.A.; Gungunes, H.;Sungur, A., and Turker, G., 2008. On the origin and age of the
Arburnu beachrock, Gelibolu Peninsula, Turkey. Turkish Journalof Earth Sciences, 17, 803819.
Erguvanl, K., 1955. Etude geologique de lile de Bozcaada. Bulletinde la Societe Geologique de France, 6(5): 399401.
Erol, O., 1972. Beachrock formations on the Gelibolu Peninsulacoast. Geographical Journal of Ankara University, (34), 12.
Ertek, T.A. and Erginal, A.E., 2003. Physical properties of beach-rocks on the coasts of Gelibolu Peninsula and their contributionto the Quaternary sea level changes. Turkish Journal of Marine
Science, 9, 3149.Folk, R.L., 1974. The natural history of crystalline calcium carbon-
ate; effect of magnesium content and salinity. Journal of Sedimen-tary Petrology, 44, 4053.
Friedman, G.M., 1964. Early diagenesis and lithification in carbon-ate sediments. Journal of Sedimentary Petrology, 34, 777813.
Friedman, G.M. and Gavish, E., 1971. Mediterranean and Red Sea(Gulf of Aqaba) beachrocks. In: Bricker, O.P. (ed.), Carbonate Ce-ments. Baltimore, Maryland: Johns Hopkins Press, pp. 1316.
Ginsburg, R.N., 1953. Beachrock in South Florida. Journal of Sedi-mentary Petrology, 23, 8592.
Gischler, E. and Lomando, A.J., 1997. Holocene cemented beach de-posits in Belize. Sedimentary Geology, 110, 277297.
Hanor, J.S., 1978. Precipitation of beachrock cements: mixing of ma-rine and meteoric waters vs. CO2 degassing. Journal of Sedimen-tary Petrology, 48, 489501.
Holail, H. and Rashed, M., 1992. Stable isotopic composition of car-
bonate-cemented recent beachrock along the Mediterranean andRed Sea coasts of Egypt. Marine Geology, 106, 141148.
Jones, B. and Kahle, C.F., 1993. Morphology, relationship, and originof fiber and dendritic calcite crystals. Journal of Sedimentary Pe-trology, 63(6), 10181031.
Kalafatcoglu, A., 1963. Geology of Ezine area and Bozcaada, the ageof limestones and serpentines. Bulletin of Mineral Research and
Exploration, 60, 6069 [in Turkish].Kayan, I., 1994. Tuzla Ovasnn (Ayvack-Canakkale) aluvyal jeo-
morfolojisi ve Holosendeki ky cizgisi degismeleri. Ege Universi-tesi Arastrma Fonu, Proje No: EDF 1988-027, 100p. [in Turkish].
Kayan, I., 1995. The Troia bay and supposed harbour sites in theBronze Age. Studia Troica, 5, 211235.
Kayan, I., 1999. Holocene stratigraphy and geomorphological evo-lution of the Aegean coastal plains of Anatolia. Quaternary Science
Reviews, 18, 541548.Kelletat, D., 2006. Beachrock as a sea-level indicator? Remarks from
a geomorphological point of view. Journal of Coastal Research,22(6), 15551564.
Khadkikar, A.S. and Rajshekkar, C., 2003. Microbial cements in Ho-locene beachrocks of South Andaman Islands, Bay of Bengal. Cur-rent Science, 84(7), 933936.
Kneale, D. and Viles, H.A., 2000. Beach cement: incipient CaCO3cemented beachrock development in the upper intertidal zone,North Uist, Scotland. Sedimentary Geology, 132, 165170.
Krumbein, W.E., 1979. Photolithotrophic and chemoorganotrophicactivity of bacteria and algae as related to beachrock formationand degradation (Gulf of Aqaba, Sinai). Geomicrobiology Journal,1, 156202.
Mabesoon, J.M., 1964. Origin and age of the sandstone reefs of Per-nambuco (Northeastern Brazil). Journal of Sedimentary Petrology,35, 715726.
Mejdahl V. and Btter-Jensen, L., 1994. Luminescence dating of ar-chaeological materials using a new technique based on single ali-
quot measurements. Quaternary Science Reviews (Quaternary Geo-chronology), 13, 551554.
Meyers, J.H., 1987. Marine vadose beachrock cementation by cryp-tocrystalline magnesian calcite-Maui, Hawaii. Journal of Sedimen-tary Petrology, 57, 755761.
Moore, C.H., 1973. Intertidal carbonate cementation, Grand Cay-man, West Indies. Journal of Sedimentary Petrology, 43, 591602.
Moore, C.H., Jr., and Billings, G.K., 1971. Preliminary model ofbeachrock cementation, Grand Cayman Island, B.W.I. In: Bricker,O.P. (ed.), Carbonate Cements. Baltimore, Maryland: John Hop-kins Press, pp. 4043.
Murray, A.S. and Roberts, R.G., 1998. Measurement of the equiva-
7/29/2019 BOZCADA NGLZCE
9/10
358 Erginal, Kyak, and Ozturk
Journal of Coastal Research, Vol. 26, No. 2, 2010
lent dose in quartz using a regenerative-dose single-aliquot pro-tocol. Radiation Measurements, 29, 503515.
Murray, A.S. and Wintle, A.G., 2000. Luminescence dating of quartzusing an improved single-aliquot regenerative-dose protocol. Ra-diation Measurements, 32, 5773.
Neumeier, U., 1998. Le role de l activite microbienne dans la cimen-tation precoce des beachrocks (sediments intertidaux). Geneva,Switzerland: University of Geneva, Thesis. Terre et Environne-ment, 12, 183p.
Neumeier, U., 1999. Experimental modelling of beachrock cemen-tation under microbial influence. Sedimentary Geology, 126, 3546.
Olley, J.M.; Murray, A.S., and Roberts, R.G., 1996. The effects ofdisequilibria in the uranium and thorium decay chains on burialdose rates in fluvial sediments. Quaternary Geochronology, 15,751760.
Prescott, J.R. and Hutton, J.T., 1994. Cosmic ray contribution todose rates for luminescence and ESR dating: large depths andlong-term time variations. Radiation Measurements, 23, 497500.
Rey, D.; Rubio, B.; Bernabeu, A.M., and Vilas, F., 2004. Formation,exposure, and evolution of a high-latitude beachrock in the inter-tidal zone of the Corrubedo complex (Ria de Arousa, Galicia, NWSpain). Sedimentary Geology, 169, 93105.
Saltk, O. and Saka, K., 1972. Geological investigation of northernSaros Gulf, Gelibolu Peninsula, Imbroz-Bozcaada and Canakkalecoastline. TPAO Archives No. 786 [in Turkish].
Schmalz, R.F., 1971. Formation of beachrock at Eniwetok Atoll. In:Bricker, O.P. (ed.), Carbonate Cements. Baltimore, Maryland:Johns Hopkins Press, pp. 1724.
Scoffin, T.P., 1970. A conglomeratic beachrock in Bimini, Bahamas.Journal of Sedimentary Petrology, 40, 756758.
Scoffin, T.P. and Stoddart, D.R., 1983. Beachrock and intertidal ce-
ment. In: Goudie, A.S. and Pye, K. (eds.), Chemical Sediments andGeomorphology: Precipitates and Residua in the Near-Surface En-vironment. London: Academic Press, pp. 401425.
Sellwood, B.W., 1995. Principles of carbonate diagenesis. In: Parker,A. and Sellwood, B.W. (eds.), Quantitative Diagenesis: Recent De-velopments and Applications to Reservoir Geology. NATO ASI Se-ries C: Mathematical and Physical Sciences 453. Dordrecht, Neth-erlands: Kluwer Academic, 286p.
Spratt, T.A.B. and Forbes, E., 1847. Travels in Lycia, Milyas, and
the Cibyratis. II. London: John Van Voorst, Paternoster Row.Spurgeon, D.; Davis, R.A., Jr., and Shinnu, E.A., 2003. Formation ofbeach rock at Siesta Key, Florida and its influence on barrierisland development. Marine Geology, 200, 1929.
Stoddart, D.R. and Cann, J.R., 1965. Nature and origin of beachrock.Journal of Sedimentary Petrology, 35, 243247.
Taylor, J.C.M. and Illing, L.V., 1969. Holocene intertidal calciumcarbonate cementation. Qatar, Persian Gulf. Sedimentology, 12,69107.
Tucker, M.E. and Wright, P., 1990. Carbonate Sedimentology. Ox-ford, UK: Blackwell Scientific Press, 482p.
Verrecchia, E.P. and Verrecchia, K.E., 1994. Needle-fiber calcite; acritical review and a proposed classification. Journal of Sedimen-tary Research, 64(3a), 650664.
Vieira, M.M. and De Ros, L.F., 2006. Cementation patterns and ge-netic implications of Holocene beachrocks from northeastern Bra-zil. Sedimentary Geology, 192(34), 207230.
Vousdoukas, M.I.; Velegrakis, A.F., and Plomaritis, T.A., 2007.Beachrock occurrence, characteristics, formation mechanism andimpacts. Earth-Science R eviews, 85, 2346.
Webb, G.E.; Jell, J.S., and Baker, J.C., 1999. Cryptic intertidal mi-crobialites in beachrock, Heron Island, Great Barrier Reef: impli-cations for the origin of microcrystalline beachrock cement. Sedi-mentary Geology, 126, 317334.
7/29/2019 BOZCADA NGLZCE
10/10
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