Controlling Factors of Recent Clastic Coastal Sediments

7/29/2019 Controlling Factors of Recent Clastic Coastal Sediments

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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
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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

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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

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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


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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)

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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)

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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

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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

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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)

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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

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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)

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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

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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

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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


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

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