controlling factors of recent clastic coastal sediments
TRANSCRIPT
-
7/29/2019 Controlling Factors of Recent Clastic Coastal Sediments
1/14
O R I G I N A L A R T I C L E
Controlling factors of recent clastic coastal sediments(Viransehir, Mersin bay, S Turkey)
Murat Gu l Ahmet O zbek Mehmet Ali Kurt
Kemal Zorlu
Received: 15 January 2008 / Accepted: 23 April 2008/ Published online: 10 May 2008
Springer-Verlag 2008
Abstract The Plio-Quaternary conglomeratic sets within
the marine environment of the Viransehir coast (W Mersin,S Turkey) are responsible for the evolution of sandy and
gravely beaches due to their control on various factors such
as sea floor irregularity, wave energy, and organic activity.
The conglomeratic sets close to the shoreline (50150 cm)
act as wave breakers, creating hard substratum and high
energy, well-oxygenated environment for organisms like
Patella sp., Phoronida worms and Brachidontes pharaonis
(Fischer P. 1870). The boring activities of these organisms
have disintegrated the sandy matrix of these sets. Finer-
grained matrix sediments have been transported to the int-
erset and open sea, while cobblepebbles have been carried
landwards and have created imbricated gravely beach
deposits without matrix. Sandy beach is evolving where the
conglomeratic sets away from the shoreline (5.010.0 m).
In this example, sets form a bar; causing fivefold division as
backshore, berm, surf zone, bar and offshore from land to
sea. Poorly sorted, cobbles-pebbles cobbles and pebbles are
found associated with the high-energy environments of
bars, whilst well-sorted sands are observed in low energeticenvironments on shore. The sets and recent shell fragments
are the main sources of coastal sediments in Viransehir.
However, the amount of shell fragments decrease towards
the active river mouth. This is due to sediment and fresh
water influx from the river causing deteriorated tempera-
ture, salinity and light penetration of the marine
environment resulting in less organic diversity.
Keywords Recent coastal sedimentation Host rock
Bioerosion Sea wave Base topography
Introduction
Large-scale sedimentation and morphology of coastal areas
are significantly influenced by tectonism and sea level
fluctuation (Galloway and Hobday 1996). However, dif-
ferent researchers have found that at the small scale,
irregular sea floor topography formed by bedrock and
wave-tidal effects are the main controls on the morphology
of the coastal areas (Leeder 1982; Friedman et al. 1992;
Reinson 1992; Galloway and Hobday 1996).
Mersin Bay is located in front of the narrow SW edge of
the Neogene Adana Basin in the Eastern Mediterranean (S
Turkey; Fig. 1). This basin has been affected by the complex
tectonic movements among the ArabianAnatolianAfrican
Plates since the Late Cretaceous period (Sengor and Ylmaz
1981; Robertson et al. 2004; Kelling et al. 2005). The
southern lowland, Post Miocene to Plio-Quaternary clastics,
caliche, limestone deposits, and drainage system are sourced
from the topographically higher northern hard MiocenePre
Miocene limestones and ophiolites of this basin (Figs. 1, 2;
Senol et al. 1998; Cobanoglu et al. 2006; Gul 2007).
Electronic supplementary material The online version of thisarticle (doi:10.1007/s00254-008-1360-7 ) contains supplementarymaterial, which is available to authorized users.
M. Gul (&)
Department of Geological Engineering, Engineering Faculty,Mugla University, 48000 Kotekli, Mugla, Turkey
e-mail: [email protected]; [email protected]
A. Ozbek
Department of Geological Engineering,
Engineering-Architecture Faculty,
Kahramanmaras Sutcu Imam University,
46100 Avsar, Kahramanmaras, Turkey
M. A. Kurt K. Zorlu
Department of Geological Engineering, Engineering Faculty,
Mersin University, 33324 Ciftlikkoy, Mersin, Turkey
123
Environ Geol (2009) 57:809822
DOI 10.1007/s00254-008-1360-7
http://dx.doi.org/10.1007/s00254-008-1360-7http://dx.doi.org/10.1007/s00254-008-1360-7 -
7/29/2019 Controlling Factors of Recent Clastic Coastal Sediments
2/14
Fig. 1 a The study area is
located in front of the Middle
Taurides region (Ozgul 1976). b
This region is situated at the SW
edge of the Adana Basin
(Kelling et al. 2005; EAF East
Anatolian Fault Zone, DSF
Death Sea Fault Zone; EF
Ecemis Fault Zone). c Satellite
view of the study area from
Google Earth (http://www.
earth.google.com. Accessed
June 2007) with the locations of
the detailed study areas and
section lines
810 Environ Geol (2009) 57:809822
123
http://www.earth.google.com/http://www.earth.google.com/http://www.earth.google.com/http://www.earth.google.com/ -
7/29/2019 Controlling Factors of Recent Clastic Coastal Sediments
3/14
The wave-dominated microtidal (Davies 1973) coasts of
Viransehir (W Mersin Bay; 5080 cm tidal range, Gul et al.2007) have sandy, gravely beaches and is fed by the active
Mezitli River. The basement of the coastal areas in
Viransehir was formed by the deltaic Plio-Quaternary con-
glomeratic sets. At the small scale (1.5 km), these sets cause
both fivefold divisions and sandy beach evolution, create
suitable hard substratum for the diverse organism (Gul et al.
2007) and lead to gravely beach evolutions. The initial aim
of this study is to clarify the composition and pattern of the
recent sedimentation and morphological changes in the Vi-
ransehir coast. Furthermore, their variations are explained in
terms of both natural and artificial, man-made structures
(wave breaker, road filling etc.). It is estimated that thenatural sets particularly controlled the wave action, clarity-
energy-substratum type of the environments and hence the
organic activity. Organic activity is dependent upon suitable
environmental conditions; however, deterioration of the
environment due to sediment and fresh water entrance from
the river may reduce the organic activity. In summary, the
objective of this study is to investigate the local controlling
factors important to the coastal sedimentation.
Regional setting
In the northern part of the study area, Palaeozoic carbona-
ceous basement rocks of the Adana basin have been found
locally (Yetis and Demirkol 1986; Unlugenc et al. 1990)
(Fig. 2). The Mesozoic of this basin includes the Triassic
clastics (Karagedik Formation), JurassicCretaceous car-
bonates (Cehennemdere Formation), Late Cretaceous
limestone and calciturbidite (Yavca Formation), Late Cre-
taceous Mersin Ophiolite and Late CretaceousPaleocene
Fndkpnar Melange (gabbro, serpentinized peridodite
pyroxenite and sedimentary blocks) (Demirtasl et al. 1984;
_Is ler 1990; Parlak and Delaloye 1996; Ozer et al. 2004;Fig. 2).
Unlugenc et al. (1990) and Gurbuz (1999) separated four
mega-sequences in the Cenozoic sequences: (1) the Kar-
sant (Oligocene lacustrine sediments) and the Gildirli
Formations (OligoceneEarly Miocene fluvial clastics); (2)
the Karaisal (Early-Middle Miocene reef limestone) and
the Kaplankaya Formations (Early-Middle Miocene clay-
stone, marl, sandy limestone); (3) the Cingoz (Middle
Miocene submarine fan clastics) and the Guvenc Forma-
tions (Middle Miocene deep marine shales); and (4) the
Kuzgun (MiddleLate Miocene reef, deltaic conglomerate,
fluvial deposits) and the Handere Formations (Late Mio-cenePliocene oolitic limestone, evaporites; Fig. 2).
The northern region of the coastal area contains the Plio-
Quaternary deposits including clayeysandygravely allu-
vial deposits, caliche and gravely red colored alluvial soil
(DSI 1978; Eren et al. 2004; Sahin et al. 2003). Upper
MiocenePliocene clastics, CalabrianTyrrhenian caliches
and conglomerates are exposed in the northwest area of the
study, whilst TyrrhenianHolocene fluvial clastics and
beach-deltaic clastics can be observed in Mezitli town and
Mersin city centrum (S enol et al. 1998; Fig. 2).
Method
This study was completed on the recent coastal sediments
in Viransehir district, 10 km W of Mersin (S Turkey) along
the Eastern Mediterranean. Three regions were recognized
in this area according to their coastal morphology and
beach sediment type. These regions are the sandy coasts of
the Pompeipolis (W) and Mezitli stream areas (E), and the
gravely beach of the Municipality Park area (central part).
Fig. 2 General geological map
of the northern part of the study
area (modified from, Erentoz
and Ternek (1962), Mineral
Research and Exploration
Institute-map: http://www.mta.
gov.tr/mta_web/500.000/image/
adana/asp)
Environ Geol (2009) 57:809822 811
123
http://www.mta.gov.tr/mta_web/500.000/image/adana/asphttp://www.mta.gov.tr/mta_web/500.000/image/adana/asphttp://www.mta.gov.tr/mta_web/500.000/image/adana/asphttp://www.mta.gov.tr/mta_web/500.000/image/adana/asphttp://www.mta.gov.tr/mta_web/500.000/image/adana/asphttp://www.mta.gov.tr/mta_web/500.000/image/adana/asp -
7/29/2019 Controlling Factors of Recent Clastic Coastal Sediments
4/14
Five divisions were delineated from the sandy beach areas
with respect to the basement topography; backshore, berm,
surf zone, bar and open sea (offshore) from land to sea. The
gravely beach includes three divisions, which are gravely
beach, natural set and interset-open sea areas from land to
sea. Twenty-four loose sediment samples were collected
from four different lines (from land to the sea) in the
Pompeipolis area, five loose sediment samples in one linefrom the Mezitli stream area plus one loose sediment and
two conglomerate rock samples from the Municipality Park
area during the field studies.
Sieve analyses of 30 samples (13603430 g) were per-
formed using eight different sieves (0,06220 mm; see
supplementary material, 1). Frequency ratios, cumulative
retained percentage and cumulative passing percentages
were calculated (see supplementary materials, 2, 3, 4) and
graphically presented in Figs. 3, 4 and 5, based on the
assumptions of Folk (1974). Total gravel, sand and
silt + clay percentages were calculated according to the
Udden (1898)Wenthworth (1922) sediment size scales
(see supplementary material, 5) and classified according to
Folk (1974) classification (Fig. 6). Some statistical
parameters such as standard deviation (mean grain size),
skewness, kurtosis and sorting were calculated (see sup-
plementary material, 5) and evaluated (Table 1) based on
the assumptions of Folk (1974). Grain size of the sediments
can be used for determining types of the depositional
environment (Sahu 1983; Ramamohanarao et al. 2003). V1and V2 discriminate functions were calculated based on
Sahu (1983) suggestions that were also reported in Ram-
amohanarao et al. (2003);
V1 0:48048X10:6231X20:40602X30:44413X4;
V2 0:24523X10:45905X20:15715X30:83931X4;
where, X1 is the mean size; X2 is the variance [square of
standard deviation (sorting)]; X3 is the skewness and X4 is
the kurtosis (see supplementary material, 5).
The compositional change of sediments in different
divisions of the sandy beach was also examined in the
Fig. 3 Sieve analysis graphs
of the Viransehir coast (Mersin,
S Turkey)
812 Environ Geol (2009) 57:809822
123
-
7/29/2019 Controlling Factors of Recent Clastic Coastal Sediments
5/14
Pompeipolis area. Five samples of approximately 1520 g
in 0.81.0 mm diameter were selected and examined under
the microscope and photographed. Five hundred points
were counted in each section and ophiolitelimestone
quartz-recent shell fragments ratios were determined
(Table 2). Two thin sections of the matrix from the Plio-
Quaternary conglomerates were also prepared and exam-
ined under the polarized microscope.
Recent shallow marine clastic sedimentation
in Viransehir coast
Three regions were studied in detail along the Viransehir
coast under the scope of this study (Fig. 1). (1) The Pom-
peipolis area, that is restricted by artificial breakwaters
(western ancient and eastern younger) (Fig. 7); (2) The
Mezitli stream area, that is limited by an artificial fill, Plio-
Quaternary deltaic deposits and recent fluvial sediment
(Fig. 8); and (3) The Municipality Park area (central part),
that is restricted by an artificial breakwater and Plio-Qua-
ternary deposits (Fig. 9). The Pompeipolis and Mezitli
stream areas were examined together due to their similar
morphological view and sedimentation pattern.
Pompeipolis area and Mezitli stream area
Five divisions have been delineated in these areas depen-
dent upon basement topography and separation in
accordance with the general research on the coastal areas
(Leeder 1982; Selley 1988; Reinson 1992; Galloway and
Hobday 1996). (1) Backshore: sandy sediments located
between the sea (landward boundary of the swash zone)
and man-made structures (road, park etc.), which are
always exposed to atmospheric conditions. It is inclined
34 through the sea. (2) Berm: it has slightly mound
shape, and includes the swash and backwash where the
backshore area meets seawater. It has an 810 inclined
slope. It stays either under the seawater or under atmo-
spheric conditions depending on wave fluctuations. (3) Surf
zone: it is relatively low inclined (461) and in the form
of a flat area between the berm and the bar. (4) Bar: it is
located 510 m away from the coast under 1.01.5 m of
seawater. Seaward inclination of this mound shaped
structure is greater than 10. Normal waves break in this
zone, and most of the wave energy is absorbed. (5) Open
sea (offshore): it starts immediately in front of the bar and
extends to the open sea with a very low 3 gradient
(Fig. 7a).
Fig. 4 Frequency curves
of the Viransehir coast (Mersin,
S Turkey)
Environ Geol (2009) 57:809822 813
123
-
7/29/2019 Controlling Factors of Recent Clastic Coastal Sediments
6/14
Backshore
Medium to coarse-grained sands are found in this division
of the Pompeipolis area. These sediments are moderate to
well sorted in the central part, whilst poorly-sorted at the
edges (Table 1; Figs. 3, 4, 5; see supplementary materials,
15). Nearly half of the coarser materials at the edges are
made up of recent shell fragments.
A bimodal sediment distribution was observed within
the Mezitli stream area (Fig. 4; See supplementary mate-
rial, 2). The first mode of this poorly sorted sediment is
cobblepebble size fragments of ophiolite and limestonegravels (Fig. 3; see supplementary material, 5). The second
mode value is medium-grained sand size with similar
composition to the first mode.
Berm
The edges of this division in the Pompeipolis area contain
poorly sorted and abundantly coarse-grained sand sedi-
ments. However, the central part includes moderate to
well-sorted and medium to fine-grained sands (Table 1;
Fig. 3; see supplementary material, 5).
Moderate to well-sorted, dominantly medium-grainedsands are found in the Mezitli stream (Table 1; Fig. 3; see
supplementary material, 5). This is similar to the central
part of the Pompeipolis area.
Surf Zone
Poorly to very poorly sorted, dominantly coarse to very
coarse-grained sands are found in the central and western
part of the Pompeipolis area, whilst pebble to granule size
Fig. 5 Cumulative retained
material percentage versus U
graph of Viransehir coast
(Mersin, S Turkey)
Fig. 6 Classification of recent coastal sediments according to theFolk (1974) classification system
814 Environ Geol (2009) 57:809822
123
-
7/29/2019 Controlling Factors of Recent Clastic Coastal Sediments
7/14
gravels dominate the eastern part (Fig. 3; see supplemen-
tary material, 5). Field observations indicated that recent
shell fragments made up approximately 20% of these
sediments.
Poorly sorted, dominantly pebble to very coarse-grained
sands were found in the Mezitli stream area. Recent shell
fragments were rarely observed in this division.
Bar
Lithified, matrix-supported and poorly to very poorly
sorted Plio-Quaternary conglomerates (mostly ophiolite
and to a lesser extent various aged limestone gravels)
have formed lenticular, mound shaped, small highs on
the sea floor. Normal waves break in this zone. Their
irregular distributions has also caused the evolution of a
second bar, located deeper and on the seaward side of
the first bar, within the Pompeipolis area. The recent
sediments over the bar include very poorly sorted,
dominantly pebble to granule gravels and very coarse-
grained sand. Fine-grained sediments have concentrated
at the edges of this division (quiet sections) due to the
absence of these bars extension (Table 1; Figs. 3, 4, 5, 6,
7). Recent shell fragments have been rarely observed in
this division.
Very poorly sorted, dominantly cobble to pebble size
ophiolite and to a lesser extent, limestone gravels were
found in the Mezitli stream area (Table 1; Figs. 3, 4, 5, 6,
7; see supplementary material, 5). The mean grain size of
this area is coarser than that of the Pompeipolis area. The
sediment types are similar to the recent embankment sed-
iments of Mezitli stream.
Open sea (offshore)
Well-sorted, medium to fine-grained sands have been
found in both of the Pompeipolis (Figs. 1, 2, 3, 4, 5, 6)
and Mezitli stream areas (Table 1; Figs. 3, 4, 5, 6; see
supplementary material, 5). This quiet environment is
located under the wave base and extends from the front of
the bars.Table1
Sorting,skewnessandcla
ssificationofeachsampleplustheirdistributionsbasedupontheirmorphologicalfea
tures
Location
Backsh
ore
Berm
SurfZone(Foreshore)
Bar(Shoreface)
OpenSea(Offshore)
SnSo
r
Sk
K
Cl
Sn
Sor
Sk
K
Cl
Sn
SorSk
K
ClSn
Sor
Sk
K
Cl
Sn
SorSk
K
Cl
Sn
SorSk
K
Cl
Pompeipolis
West
2
P
NS
MK
(g)S
1
P
SF
MK
gS
22
P
F
LK
gS
23
P
NS
LK
gS
24
M
SF
MK
(g)S
3
MW
SF
MK
S
Middle
5
M
F
PK
S
4
M
F
MK
S
18
P
F
VL
gS
19
P
F
PK
sG
20
VP
SF
PK
sG
21
M
SF
MK
S
East
7
M
W
SF
MK
(g)S
6
W
F
VK
S
13
M
F
MK
gS
14
P
NS
MK
sG
15
VP
F
PK
sG
17
M
SF
MK
S
16
P
F
MK
sG
Easternmost9
P
F
PK
gS
8
P
NS
PK
(g)S
10
P
SF
LK
sG
11
MW
SF
MK
(g)S
12
VP
SF
VL
sG
Munipicality
25
M
SF
VK
S
Mezitlistreamarea
26VP
SF
PK
sG
27
MW
C
LK
(g)S
28
P
C
MK
sG
29
P
SF
PK
G
30
M
SF
MK
S
SorSorting,
Ppoorlysorted,
VPv
erypoorlysorted,
M
moderatelysorted,M
W
moderatelywellsorted;SkSkewness,F
fineskewed,
VFveryfineskewed,
NSne
ar-symmetrical,Ccoarse
skewed;KKurtosis,VKveryplaty
kurtic,
PKplatykurtic,
MKmesokurticnearlysymmetrical,LKleptokurtic,
VLvery
leptokurtic;(g)Sslightlygravellysand,gS
gravellysand,sGsandy
gravel,
Ssand,
Ggravel,
ClsedimentclassificationbasedonFolk(1974),sam
plenumber
Table 2 Provenance results of the western section in the Pompeipolis
Area
Location Sample No Ophiolite Limestone Quartz Recent shell
debris
Backshore 2 81.7 7.9 4.3 6.1
Berm 1 42.6 20.9 8.1 28.4
Surf Zone 22 63.7 7.4 5.7 23.2Bar 23 68.5 10.0 6.5 15.0
Open Sea 24 41.5 14.3 5.8 38.4
Environ Geol (2009) 57:809822 815
123
-
7/29/2019 Controlling Factors of Recent Clastic Coastal Sediments
8/14
Municipality Park area
The sedimentation and morphologic appearances of this
area are completely different from sandy areas above-
mentioned (Figs. 9, 10). The divisions of the other twoareas have not evolved in this region. Three separate
divisions have been delineated in this area (Fig. 10). (1)
Gravely beach: This is located between the natural
coastal line and a park filling area (Fig. 10d). (2) Natural
set: it is formed by lithified, matrix-supported and poorly
to very poorly sorted Plio-Quaternary conglomerates.
They have an irregular distribution with flat top surfaces
that are very close to the sea surface and often exposed
as well as cliff side surfaces (Fig. 10ac). (3) Open sea
and interset area: an interset area is located among the
natural sets and open sea areas with similar properties
to the open sea (offshore) division of the previous
regions.
Gravely beach
This division includes very poorly sorted and moderately
imbricated, cobble to pebble size gravels dominated by
ophiolite and to a lesser extent limestone without matrix
(which can also be classified as sieve deposit) (Table 1;
Figs. 3, 4, 5, 6, 10d; see supplementary material, 5). The
clasts have a similar composition to the natural set
conglomerates.
Fig. 7 a General view of the
Pompeipolis area. b Cross
section from land to the open
sea. c Close view of the Plio-
Quaternary conglomerates of
the bar division (scale 18 cm). d
The wire mesh application used
to determine the relative
proportions of the components
of sample 24 (O ophiolite rock
fragments, R recent shell debris,
Llimestone fragments, Q quartz
detrials)
816 Environ Geol (2009) 57:809822
123
-
7/29/2019 Controlling Factors of Recent Clastic Coastal Sediments
9/14
Natural set
The flattened top of the natural sets is generally covered
by 010 cm of seawater during normal daily conditions.
However, these areas become covered by 3050 cm of
water during high tide (Fig. 10a, b), and are exposed
during low tide. Laterally discontinuous deltaic con-
glomerates mainly consist of ophiolite and to a lesserextent limestone gravels. Their sizes range from 3 to
25 cm. Medium to coarse-grained sands (with little calcite
cement) binds these gravels. Those sets act as wave
breaker and form a clear, high energetic, well light pen-
etrated, warm environment for organisms. Limpet Patella
sp., Phoronida worms and bivalve Brachidontes pharaonis
(Fischer P. 1870) are mostly found over the loose matrix
(Fig. 10b, c).
The conglomerates have been disintegrated as a result of
the boring, hollowing and feeding activities of these
organisms. As a result, the finer-grained sediments have
been released and carried to the open sea and interset areas,whilst the gravels have been transported to the land by sea
waves forming imbricated, gravely beach deposits. Varia-
tion of the organism activities, strength differences in the
conglomerate and local environmental conditions have
produced rough top surfaces (Fig. 10).Fig. 8 a General view of the Mezitli stream area. b Field view of the
man-made embankment formed using recent sediment input from the
Mezitli stream (Scale 1.70 m)
Fig. 9 a General view of the
Municipality Park area. b Cross
section of the Municipality Park
area
Environ Geol (2009) 57:809822 817
123
-
7/29/2019 Controlling Factors of Recent Clastic Coastal Sediments
10/14
Open sea (offshore) and interset area
These areas are relatively quiet environments where there
are limited or no wave effects. Moderately sorted, strongly
fine skewed, mostly medium-grained sand and to a lesser
extent finer-grained sands were observed in this division
(Table 1; Figs. 3, 4, 5, 6; see supplementary material, 5).
Controlling factors of the recent coastal sedimentation
In addition to the host rock, sediment type, wave energy,
fresh water and sediment input plus organic activity were
determined as controlling factors on the recent coastal
sedimentation pattern in the Viransehir coast.
Host rock
Plio-Quaternary deltaic-coastal sediments have an irregular
distribution in the shallow marine environment of the
Mersin Bay. They have formed irregular sea floor topog-
raphy, sets and bars (Figs. 7, 9, 10). Conglomeratic bars
away from the coastline created five divisions and resulted
in the formation of sandy beaches. However, flat-topped
conglomeratic sets close to the coastline formed a suitable
hard substratum for organisms, which caused the formation
of gravely beaches. All of these topographic highs act as
wave breaker, which effectively control the energy of the
environment, light penetration, temperature and hence
organic activities in the study area. Macroscopic and
microscopic examinations indicated that the recent sedi-
ments have a similar composition to the host rocks.
Sediment type
The sediment source in the study area is located in the
north of the Mersin Bay, and consists of ophiolite and
various aged limestone. Plio-Quaternary deltaic-coastal
sediments and recent alluvial sediments around the stream
contain the fragments of these materials. Reworked mate-
rials of the Plio-Quaternary conglomerates (due to wave
action and organic activities) are the main source of the
recent coastal sediments of the Virans ehir coast.
Four different components (ophiolite, limestone, quartz,
recent shell fragments) were counted under the microscope
in order to show the compositional changes of the division.
Fig. 10 a Close view of the Plio-Quaternary conglomerates (O
ophiolite rock fragments; L burrowed limestone; Mx medium to
coarse-grained sand matrix; scale 18 cm). b The conglomeratic
natural set covered by 010 cm of seawater during normal daily
conditions, large cobbles of sets are exposed (Scale 1.70 m). c Close
view of the exposed cobbles of natural set. Different types of
organism are tightly attached to the cobble surface, whilst relatively
soft matrix is completely covered by the same type of organism [O
ophiolite rock fragments; L limestone fragment; Mx Matrix; M
Brachidontes pharaonis (Fischer P. 1870); G Patella sp.]. d Boring
and hollowing activities of organisms have disintegrated the con-
glomerates, cobble to pebble size gravels are transported landwards
and form imbricated (arrow to the north) gravely beach-sieve deposit
(Scale 50 cm)
818 Environ Geol (2009) 57:809822
123
-
7/29/2019 Controlling Factors of Recent Clastic Coastal Sediments
11/14
Ophiolitic rock fragments are heavier than the other com-
ponents due to their higher mineral density content such as;
nickel, chromium and iron. Thus, cobble and pebble sized
fragments of ophiolites cannot be carried for long dis-
tances, and were immediately deposited in front of the bar
(Pompeipolis area) or transported for very short distances,forming a gravely beach (Municipality Park area). Recent
shell fragments were formed by the fragmentation of the
shallow marine organisms. They are lighter than the other
components. Thus, relative ratios of the various aged
limestone and recent shell fragments are increasing in surf
zone and berm areas (especially at edges restricted by the
breaker), however, they are easily decomposed under
atmospheric conditions, and become less important in the
backshore area (Table 2; Fig. 11). Quartz is the most
durable mineral, however, it is one of the less dominant
components in the recent coastal sediments of the Vi-
ransehir coast due to its absence from the source and the
short transportation distances involved.
Wave energy
In coastal regions, finer-grained sediments are deposited
within the low energy and gently inclined areas, whilst
coarse-grained sediments are deposited in the narrow areas
where the wave energy is high (Galloway and Hobday
1996). The average wave height (NWSE directed) of the
Mersin Bay is less than the 1 m (http://www.meteoroloji.
gov.tr, Republic of Turkey Ministry of Environment and
Forestry Turkish State Meteorological Service. Accessed
Sept 2007). The annual average wind speed is around the
2.3 m/s. The strongest wind has 28.2 m/s. The primary
dominant wind direction is NNW to SSE, whilst the second
most dominant wind direction is SSW to NNE (Mersin
Province 2005). However, there is no significant or strong
wave and wind action observed in the study area. Most of
the open sea conditions (large sea waves) due to strong
wind effects are damped by the shallowing sea floor
topography and coastal morphology. The Plio-Quaternary
rock bars far away from the coastline have absorbed
the residual wave energy and resulted in a high-energy
environment.
The conglomerates of these bars get progressively dis-
integrated by the wave action. Therefore, pebble to cobble
size gravels are deposited locally on site. Pebble to medium
to coarse-grained sands has been transported landwards
(surf zone, berm and backshore), whilst medium to fine-grained sediments have been carried towards the open sea
(Fig. 7). Man-made embankments, fillings and artificial
breakwaters have behaved like bars by also breaking waves
(Figs. 7, 8). Accordingly, poorly sorted, pebble to coarse-
grained sand size sediments are found in front of these
artificial structures, whilst well-sorted, finer-grained sedi-
ments were found in the central part of the study areas far
away from the artificial structures (Table 1; Figs. 3, 4, 5, 6;
see supplementary material, 5).
The energy of the environment can control the sorting
and skewness of the sediments. Well sorted and fine to
strongly fine skewed fine-grained sediments are the prod-ucts of a low energy environment (Fig. 12). On the
contrary, the coarser grains of the higher energy environ-
ments show are much more poorly sorted (Fig. 12).
Kasper-Zubillaga and Carranza-Edwards (2005), also
obtained similar observations for dune-coastal sediments in
northwestern Mexico. They pointed out that the finer-
grained sediments were well sorted in comparison to the
coarser-grained sediments in that area.
Multivariant discriminant functions of Sahu (1983) were
applied to determine the relation between the grain size and
the depositional environment (Fig. 13; see supplementary
material, 5). Some samples were not involved due to their
low V2 values (samples no: 12, 15, 20, 26 and 29). Most
samples were dropped in the beach section on the diagram
(Fig. 13). However, some deflections were determined.
Due to the highly energetic environment, the bar and surf
zone samples dropped into the turbidite section on the
diagram, while some samples of the open sea environment
dropped into the aeolian environment due to well sorting
(Fig. 13). The success of the depositional environment
determination was significantly higher than the Ramamo-
hanarao et al. (2003) application that mostly included the
river samples that dropped into the turbidite section.
Fresh water and sediment input
Recent shell fragments were rarely found in the Mezitli
stream area. The reason for this is the unsuitable conditions
for the development of these organisms. The fresh water
entrance from the Mezitli stream decreases the salinity and
temperature of the sea at the mouth of the stream. Simul-
taneously, the sediment input in this area decreases the
limpidity and light penetration of the environment. As a
Fig. 11 Sediment distributions in the divisions of the Pompeipolis
area
Environ Geol (2009) 57:809822 819
123
http://www.meteoroloji.gov.tr/http://www.meteoroloji.gov.tr/http://www.meteoroloji.gov.tr/http://www.meteoroloji.gov.tr/ -
7/29/2019 Controlling Factors of Recent Clastic Coastal Sediments
12/14
result, shallow marine organisms have not flourished as
compared to the other study areas.
Organic activity
Several types of organisms such as algae, sponges, bivalves,
pelecypods and echinoids are known as rock destroying
organisms in shallow marine environments (Friedman et al.
1992; Galloway and Hobday 1996). Most of these organ-
isms have preferentially developed over the hard substrate
formed by coarse sand to lithified beds (Taylor and Wilson
2003). Limpet Patella sp., Phoronida worms and bivalve
Brachidontes pharaonis (Fischer P. 1870) have attached to
the hard substrate of conglomerates within the Municipality
Park area. Boring, hollowing, feeding and other activities of
these organisms have disintegrated the soft matrix of these
conglomerates (Gul et al. 2007). Decomposition of the
matrix has released the gravels with the finer-grained sed-
iments being transported to the open sea and interset areas,
whilst most of the cobble and to a lesser extent, pebble size
gravels have been carried landwards to form gravely beach
deposits (sieve deposits; Fig. 10).
The study indicates the effects of the natural processes
(under the shade of the artificial structures) on the coastal
morphology, evolution and accumulation of the recent
coastal sediments in a short distance (1.5 km). The exam-
ined region is the nearest and partially preserved coastal
area, close to the Mersin city center. Similar sedimentation,
patterns were observed in the eastern part of the study area
until the end of the 1990s.
After then, the Mersin Municipality filled nearly 10 km
long coastal areas with limestone armor plates, creating
large recreational areas. In addition, the Mersin Marina, the
Mersin Port, several breakwater constructions and road
fillings have also been constructed. These artificial man-
made structures significantly affect the intensity and
direction of the sea waves and sediment circulation (Dirik
et al. 2006; Gul et al. 2008). They have also caused new
destructive erosional regions and constructive depositional
areas along the Mersin coasts (Dirik et al. 2006). Con-
structional activities along the coastal area are progressing
towards the SW of the Mersin, in which there are long
sandy beaches important for tourism. In order to protect
these regions, the local variable dynamic conditions must
Fig. 12 Graphs of sorting
versus mean grain size, sorting
versus skewness, and skewness
versus mean grain size, in the
Viransehir coast (Mersin, S
Turkey)
Fig. 13 Multivariant discrimination functions plots of the Viransehir
coastal sediments based on Sahu (1983) for determining the grain
size-depositional environment relation
820 Environ Geol (2009) 57:809822
123
-
7/29/2019 Controlling Factors of Recent Clastic Coastal Sediments
13/14
be understood. The effects of coastal constructions on
natural conditions must be clarified prior to any construc-
tion activities.
Conclusion
This study has indicated that the controlling factors onsedimentation in coastal areas can vary over short dis-
tances. The distribution of strong host rocks and man-made
structures (breakwater, fillings) have significantly affected
the basement topography and coastal morphology. Both
artificial and natural obstacles may control the direction
and intensity of the sea waves. Coarse-grained (cobble to
pebble), poorly sorted sediments were deposited in high
energy, wave-breaking environments whilst well-sorted
and finer-grained sediments (sand) are the products of
quieter environments.
Shallow marine organisms have flourished in warm,
clear, light penetrated, suitably saline environments,which are mostly over the topographic highs in shallow
marine environments. Fresh water and sediment input
from the active river can deteriorate this fragile system
and prevent the development of the organisms, causing a
decrease of shell fragments in close coastal sediments.
Boring and hollowing activities of the organisms may
destroy the hard substratum causing the formation of
gravely beaches and the supply of finer-grained sediments
to the open sea. Therefore, at the small scale the host
rock, sediment input, fresh water input, organic activity
and wave action become more important factors related to
recent coastal sedimentation than the general, broader
scale, controlling factors, such as tectonic activity, sea
level change and climate.
Acknowledgments The authors warmly thank Dr. Luke Mortimer
(Centre for Groundwater Studies, Flinders University, Australia) and
Dr. Naci Emre Altun (from Mugla University, Turkey) for their
valuable editorial reviews of the manuscript.
References
Cobanog
lu_
I, O
zbek A, Gul M (2006) Geotechnical evaluations ofbuildings over the Pleistocene-Recent loose deposits: a case
study from Mersin. 30. anniversary Fikret Kurtman Geology
Symposium, Department of Geological Engineering, Selcuk
Unversity (Konya-Turkey), pp 233234 (in Turkish with
English abstract)
Davies JL (1973) Geographical variation in coastal development.
Hafner Publ Co., New York, 204 p
Demirtasl E, Turhan N, Bilgin AZ, Selim M (1984) Geology of the
Bolkar Mountains. International symposium on the geology of
the Taurus Belt, Ankara, pp 125141
Dirik K, Leloglu UM, Tunal E, Ercanoglu M, Ozaner S, (2006) A
Development of the low coast visualization based surveying
system in order to monitoring the natural and anthropogenic
changes in Kazanl-Anamur (_Icel). The Scientific and Technical
Research Council of Turkey, Project No: CAYDAG 101Y103,
49 p (unpublished in Turkish with English Abstract)
DSI (1978) Hydrogeological investigation report of Mersin-Berdan
and Efrenk plains. General Directorate of State Hydraulic
Works, Ankara, 60 p (unpublished, in Turkish)
Eren M, Kadir S, Hatipoglu Z, Gul M (2004) Caliche development in
Mersin region. The Scientific and Technological Research
Council of Turkey, Research Project No: YDABAG102Y036,
p 55 (unpublished, in Turkish with English abstract)
Erentoz C, Ternek Z (1962) MTA (Institute of Mineral Research and
Exploration) 1/500.000 scaled general geological map of the
Adana region. (eds), Ankara. http://www.mta.gov.tr/mta_web/
500.000/image/adana.asp. Accessed Sept 2007
Folk RL (1974) The petrology of sedimentary rocks. Hemphill
Publishing Co., Austin, 182 p
Friedman GM, Sanders JE, Kapaska-Merkel DC (1992) Principles of
sedimentary deposits, stratigraphy and sedimentology. MacMil-
lan Publishing Company, UK, 717 p
Galloway WE, Hobday DK (1996) Terrigenous clastic depositional
systems, applications to fossil fuel and groundwater resources.
Springer, Heidelberg, 489 p
Gul M (2007) Effects of antecedent topography on reefal carbonate
deposition: Early-Middle Miocene of the Adana Basin, S
Turkey. J Asian Earth Sci 31(1):1834
Gul M , Ozbek A, Karayakar F, Kurt M A (2007) Biodegradation
effects over different types of coastal rocks. Environ Geol
International J Geosci. doi:10.1007/S00254-007-1110-2 (in
press)
Gul M, Ozbek A, Karayakar F, Kurt M A (2008) Recent biologic
factors effects on the Mersin Bay (S Turkey) coastal morphol-
ogy. In: Proceedings of 61th Geological Congress of Turkey
Proceedings, Ankara, Turkey, pp 142143
Gurbuz K (1999) Regional implications of structural and eustatic
controls in the evolution of submarine fans: an example from the
Miocene Adana Basin, Southern Turkey. Geol Mag 136(3):311
319_Isler F (1990) Geology of the ophiolite in the Fndkpnar (Mersin).
Cumhuriyet University J Eng Ser A Geosound 67(12):4553
(in Turkish with English abstract)
Kasper-Zubillaga JJ, Carranza-Edwards A (2005) Grain size discrim-
ination between sands of desert and coastal dunes from
northwestern Mexico. Rev Mex Cienc Geol 22(3):383390
Kelling G, Robertson AHF, Buchem FV (2005) Cenozoic sedimen-
tary basins of southern Turkey: an introduction. Sediment Geol
173(14):113
Leeder MR (1982) Sedimentology, process and product. Chapman
and Hall, USA, 344 p
Mersin Province (2005) Republic of Turkey Ministry of Environment
and Forestry. Provincial Directorate of Environment and
Forestry. Report of Mersin Province Environment Condition in
2004 (2004 yl Mersin _Il Cevre Durum Raporu) Mersin, 252 p
(in Turkish)Ozer E, Koc H, Ozsayar T (2004) Stratigraphical evidence for the
depression of the northern margin of the Menderes-Tauride
block (Turkey) during the Late Cretaceous. J Asian Earth Sci
22:401412
Ozgul N (1976) Some basic geologic properties of the Taurides. Geol
Bull Turkey 19:6579 (in Turkish with English Abstract)
Parlak O, Delaloye M (1996) Geochemistry and timing of post-
metamorphic dyke emplacement in the Mersin Ophiolite
(southern Turkey): new age constraints from40
Ar/39
Ar geochro-
nology. Terranova 8:585592
Ramamohanarao T, Sairam K, Venkateswararao Y, Nagamalleswar-
arao B, Viswanath K, (2003) Sedimentological characteristics
Environ Geol (2009) 57:809822 821
123
http://www.mta.gov.tr/mta_web/500.000/image/adana.asphttp://www.mta.gov.tr/mta_web/500.000/image/adana.asphttp://dx.doi.org/10.1007/S00254-007-1110-2http://dx.doi.org/10.1007/S00254-007-1110-2http://www.mta.gov.tr/mta_web/500.000/image/adana.asphttp://www.mta.gov.tr/mta_web/500.000/image/adana.asp -
7/29/2019 Controlling Factors of Recent Clastic Coastal Sediments
14/14
and depositional environment of Upper Gondwana rocks in the
Chintalapudi sub-basin of the Godavari valley, Andhra Pradesh,
India. J Asian Earth Sci 21:691703
Reinson GE (1992) Transgressive barrier island and estuarine
systems. In: Walker RG, James NP (Eds.) Facies models;
response to sea level change. Geological Association of Canada,
pp 179194
Robertson AHF, Unlugenc UC, _Inan N, Tasl K (2004) The Misis-
Andrn Complex: a Mid- Tertiary melange related to late- stage
subduction of the Southern Neotethys in S Turkey. J Asian Earth
Sci 22:413453
Sahu BK, (1983) Multigroup discrimination of depositional environ-
ments using size distribution statistics. Indian J Earth Sci 10:20
29
Selley RC (1988) Applied Sedimentology. Academic Press, London,
446 p
Sahin S, Boke N, Yalcn N, Mengeloglu MK (2003) The Geologic
properties of the _Icel Province). General Directorate of Mineral
and Exploration Institute, Eastern Mediterranean District Office
(Adana-S Turkey), research project, 18 p (unpublished, in
Turkish)
Sengor AMC, Ylmaz Y (1981) Tethyan Evolution of Turkey: A Plate
Tectonic Approach. Tectonophysics 75:81241
Senol M, Sahin S, Duman T, Albayrak S , Akca _I, Tas kn S (1998) the
Geological investigation report of Adana-Mersin region. General
Directorate of Mineral and Exploration Institute, Eastern Med-
iterranean District Office (Adana, S Turkey), research project, 46
p (unpublished, in Turkish)
Taylor PD, Wilson MA (2003) Palaeoecology and evolution of
marine hard substrate communities. Earth Sci Rev 62:1103
Udden JA (1898) Mechanical composition of wind deposits, vol 1.
Augustana Library Publication, Rock Islands
Unlugenc UC, Kelling G, Demirkol C (1990) Aspects of basin
evolution in the Neogene Adana Basin, SE Turkey. In: Savascn
MY, Eronat AH (eds) Proc Int Earth Sci Cong on Aegean
Region, _Izmir, vol1. pp 353370
Wenthworth CK (1922) A scale of grades and class terms for clastic
sediments. J Geol 30:377392
Yetis C, Demirkol C (1986) Detailed geologic investigation of the
western part of the Adana Basin. General Directorate of Mineral
and Exploration Institute, research project: 80378037a, 187 p
(unpublished, in Turkish)
822 Environ Geol (2009) 57:809822
123