New Present Environmental Status of the Shuaiba Lagoon, Red Sea … · 2011. 12. 28. · Present Environmental Status of the Shuaiba Lagoon, Red Sea Coast, Saudi Arabia 161 mainly

JKAU: Mar. Sci., Vol. 22, No. 2, pp: 159-179 (2011 A.D. / 1432 A.H.)

DOI : 10.4197/Mar. 22-2.9

159

Present Environmental Status of the Shuaiba Lagoon, Red

Sea Coast, Saudi Arabia

Ramadan H. Abu-Zied, Rashad A. Bantan and

Mohamed H. El Mamoney

Marine Geology Department, Faculty of Marine Science, King Abdulaziz

University, P.O.Box 80207, Jeddah 21589, Saudi Arabia email: [email protected]

Abstract. Shuaiba Lagoon is located about 80 km south of Jeddah city,

Saudi Arabia. Its environmental characteristics were determined. The

macro-fauna and flora were also sampled and identified. Extreme

values for salinity (60‰) and water temperature (33°C) were recorded

and that may be due to its shallowness and small volume and

occurrence under arid warm climate. Lagoon water pH was low (8.3),

likely, as a result of re-mineralization of organic matters. These

extreme variables exerted probably a stressful natural environment on

the calcareous macro-fauna (molluscs and corals) as indicated by

dominance of gastropod Cerithidea pliculosa and pelecypod Mytilus

edulis in the lagoon. Corals could not tolerate these conditions so they

were only recorded close to the inner- and outside inlet of the lagoon.

On the contrary, these environmental conditions are probably

favorable for mangroves, seagrasses and macro-algae (and

Cyanophytes) as indicated by their proliferation in the lagoon.

Keywords: Seagrasses, Cyanophytes, Hypersaline, Corals, Intertidal

Area, Inlet.

Introduction

Shuaiba lagoon is located about 80 km south of Jeddah city (Saudi

Arabia) on the eastern Red Sea coast, with a total area of approximately

14.3 km2

(this study). It is situated between latitudes 20° 42′ to 20° 51′ N

and longitudes 39° 26′ to 39° 32′ E (Fig. 1). It has an elongated shape

with long axis (8 km length) parallel to the Red Sea coast and a

160 Ramadan H. Abu-Zied et al.

maximum width of 3 km (Fig. 1). The Shuaiba Lagoon is connected with

the Red Sea via a narrow, deep inlet (mouth) that is located at its

southern side (Fig. 1). At its northern side, there is a narrow, shallow

tidal creek connecting it with a smaller lagoon. But this tidal creek has

been closed by artificial alluvium due to road construction. A

considerable part of the Shuaiba Lagoon area (10%) is covered by

mangroves (total area of 1.42 km2) with a height of ~3 m (Fig. 1).

The Shuaiba Lagoon is a back-reef lagoon. Its western side is

bordered by old, raised coral reef terraces, probably of Pleistocene age

(Skipwith, 1973; Al-Sayari and Zotl, 1978; Bahafzallah and El-Askary,

1981; El-Sabrouti, 1983; Behairy, et al., 1987; and Al-Washmi, 1999)

with elevations ranging from 1 to 3 m a.s.l. These raised terraces make a

natural condition protecting the lagoon from strong waves, therefore

many mangroves are able to survive and develop (Hariri, 2008). The

other sides of the lagoon are bordered by low land (0.5-1 m a.s.l) which

are composed of sand-sized alluvium and sabkha. Tidal range at the

Shuaiba Lagoon is very small similar to that of the central Red Sea (25

cm), see Lisitzin (1974). It is semi-diurnal generated by tidal force in the

Red Sea and co-oscillating tide of Gulf of Aden (Al-Barakati, 2010).

The Shuaiba Lagoon is one of the Red Sea coastal lagoons that

break the continuity of the Pleistocene reef complexes and remain as

remnant of much larger body of water (Al-Washmi, 1999). It was formed

by erosion in the pluvial Pleistocene and drowned by post glacial sea

level rise during the Holocene (Braithwaite, 1987; and Brown et al.,

1989). Occurrence of raised coral reef terraces (Pleistocene age) in the

western side of the Shuaiba Lagoon might indicate that it is a remnant of

a Pleistocene back-reef system filled by Red Sea water during the

Holocene transgression. However, Rabaa (1980) suggested that some

lagoons of the Red Sea were probably formed as a result of collapse

structures resulting from the selective solution of Miocene evaporite beds

underlying the younger succession.

Many studies (e.g., Ahmed and Sultan, 1992; Al-Washmi and

Gheith, 2003; Hariri, 2008; and Al-Barakati, 2010) have dealt with the

Shuaiba Lagoon in regard to its meteorology and water circulation,

diagenesis of sediments and microfossils, but no attention has been paid

to its environmental characteristics. Ahmed and Sultan (1992) reported

that the exchange of water between Shuaiba Lagoon and the Red Sea was

Present Environmental Status of the Shuaiba Lagoon, Red Sea Coast, Saudi Arabia 161

mainly forced by the local winds, whereas seasonal mean sea level

variations did not have a significant effect on the flushing of this lagoon.

However, Al-Barakati (2010) concluded that water circulation in the

Shuaiba Lagoon is mainly dominated by tidal force. Al-Washmi and

Gheith (2003) concluded that the coastal sabkha sediments of Shuaiba

lagoon have undergone diagenetic processes due to dominance of

dolomitic minerals. Hariri (2008) studied the benthic foraminifera of

bottom sediments of the Shuaiba Lagoon and suggested that they were

mainly controlled by factors such as: water depth, light, sediment grain

size and freshwater inputs.

Fig. 1. A map showing the Shuaiba Lagoon and stations sites (plus sign). Mangroves are

indicated by black areas.


The main objective of this study is to measure the prevailing

environmental parameters (e.g., water depth, temperature, salinity and

pH), assess their impact on the macro-fauna and flora of the Shuaiba

Lagoon and their inter-relationship, if possible, with the prevailing arid,

warm conditions.

Materials and Methods

Fifty two stations were selected for sediment samples and

measured for the environmental parameters such as water depth,

temperature, salinity and pH. At each station, macro-fauna and flora

were also separated and described. Temperature, salinity, pH and

dissolved oxygen for the lagoon surface water were measured, in situ,

during May 2010 using Hach HQ40D a multi-parameters meter. High

salinity water samples were diluted with known-volume distilled water

before measurement. Only Temperature and salinity were measured for

the water column at some stations. Water depth was measured using a

graduated bar. All of these measurements and their coordinates (assigned

by Garmin II GPS) were listed in Table 1.

Table 1. Stations coordinates, measured environmental parameters (May 2010) and main

type of macro-fauna and flora in Shuaiba Lagoon.

Sample No Latitude

(N)

Longitude

(E)

Depth

(m) pH

Salinity

(surface, ‰)

Temperature

(surface, °C) Macro-fauna and flora

SH1 20.73333° 39.49137° 0.25 8.35 46.4 29.8

SH4 20.73327° 39.49178° 1.2 8.43 43.2 29.7

SH5 20.73333° 39.49123° 0.15 8.34 47.8 30.1

SH6 20.73757° 39.48647° 0.35 8.35 49 30.1 Algae

SH7 20.7379° 39.48683° 0.5 8.38 48 29.6

SH8 20.7379° 39.48683° 0.5 8.38 48 29.6 Seagrasses

SH9 20.73817° 39.48747° 1 8.41 45.8 29.3 Seagrasses

SH10 20.7447° 39.4785° 0.2 8.36 46.2 33.7 Algae

SH11 20.7455° 39.47947° 0.7 8.41 45.4 32.9 Seagrasses

SH11B 20.7455° 39.47947° 0.7 8.41 45.4 32.9 Seagrasses

SH12 20.74593° 39.480846° 1.5 8.42 45.2 30.2 Seagrasses and algae

SH13 20.75577° 39.46832° 0.1 8.39 61.6 30.7 Algae



SH16 20.76483° 39.45897° 0.15 8.42 61 30.2 Small molluscs

SH17 20.7645° 39.46113° 0.25 8.39 49.4 30.7 Small molluscs



SH20 20.7786° 39.45832° 1 8.22 53.3 33.7 Small molluscs




SH24 20.77277° 39.47965° 0.3 8.3 52.8 31.3 Algae


Sample No Latitude

(N)

Longitude

(E)

Depth

(m) pH

Salinity

(surface, ‰)

Temperature

(surface, °C) Macro-fauna and flora

SH25 20.77371° 39.47966° 0.15 8.42 54.1 33.3 Algae

SH26 20.76134° 39.49425° 0.7 8.37 58 31.2 Small molluscs



SH29 20.74456° 39.50339° 0.2 8.46 46 33.2


SH30A 20.74473° 39.50211° 0.7 8.51 45.8 Seagrasses and algae

SH31 20.73866° 39.49544° 0.8 8.52 43 31 Coral and algae

SH31A 20.73866° 39.49544° 0.8 8.52 43 31 Coral and algae

SH32 20.72791° 39.48546° 0.3 8.5 40.9 30.8 Coral and algae



SH35 20.73807° 39.47749° 0.6 8.6 39 33.2 Coral and algae

SH36 20.73856° 39.47801° 0 8.6 39 33

SH37 20.7648° 39.48666° 0.3 8.2 48.9 32.5 Algae

SH38 20.75925° 39.49547° 0.1 8.25 56.3 33.4

SH39 20.7328° 39.49982° 0.45 8.51 41.5 32.5

SH39B 20.72852° 39.48865° 6.75 8.45 38.3 28.7

SH40 20.73097° 39.47945° 15 8.48 38.3 29.3

SH41 20.72572° 39.48278° 7 8.62 38.3 30.5

SH42 20.73355° 39.49379° 2 8.5 38.4 29.2

SH43 20.73856° 39.49135° 2 8.43 39.1 29.9

SH44 20.74444° 39.49119° 2.5 8.53 40.9 29.2 Algae

SH45 20.74679° 39.4966° 2.7 8.51 40.3 29.1 Algae

SH46 20.74696° 39.49325° 1.8 8.54 42.7 29.3 Algae

SH47 20.75085° 39.48991° 1.7 8.52 43.2 29.5 Algae

SH48 20.75206° 39.48216° 2.2 8.48 46.4 30.3 Algae




Results

1- Bathymetry

Shuaiba Lagoon is a shallow basin with the depth ranging from 1 m

(max.) in the north and 3 m (max.) in the south. Its northern part is very

shallow (~0.4 m) showing a maximum depth of 1 m at its centre (Fig. 1).

The southern part of the lagoon is the deepest part in the lagoon (~3 m).

The northern and southern parts of the lagoon are separated by a wide,

shallow tidal flat with a sand-sized shoal that is entirely populated by

mangrove trees (~3.5 m height) (Fig. 2). Immediately before the inner

inlet (mouth) of the lagoon, depth varies from 1 to 1.5 due to occurrence

of raised substrates. After that, depth increases rapidly reaching 7 m

throughout the inlet and continues to reach more than 15 m in the outer

part of the inlet (Fig. 2).


Fig. 2. Bathymetry map of the Shuaiba Lagoon. Isobath interval is 0.5 m.

2- Temperature

Surface water temperature of the lagoon’s inlet and the southern

part of the lagoon is the lowest ranging from 29 to 30° C (Fig. 3). This

(low temperature) surface water is remarkably traceable at the central

part of the lagoon, indicating the movement of Red Sea water as surface

inflow into the most parts of the lagoon (Fig. 3). In the northern part of

the lagoon, the surface water temperature increases to a high value of

~33° C (Fig. 3). It is also high (>31° C) at areas close to the lagoon’s

beaches, especially at the eastern and western sides (Fig. 3).


Fig. 3. Distribution pattern of surface water temperature in the Shuaiba Lagoon during

May 2010. Contour interval is 0.4° C.

3- Salinity

Surface water salinity of the Shuaiba Lagoon follows the pattern of

surface water temperature. In general, it is very high with a mean value

of 47‰±6. At the inlet (mouth), it shows a value of 39‰ indicating the

presence of Red Sea surface water (Fig. 4). Then, it increases gradually

inwards the lagoon until it reaches its maximum (56‰) at the northern

part of the lagoon. This indicates that inside the lagoon, the surface water

moves towards the north. The surface water salinity becomes very high


(> 50‰) in the areas that are close to the lagoon’s beaches, especially at

the eastern and western sides (Fig. 4).

Fig. 4. Distribution pattern of surface water salinity in the Shuaiba Lagoon during May

2010. Contour interval is 1.

4- pH

Surface water pH of the Shuaiba Lagoon shows, in general, a weak

negative relationship with the surface water salinity and no relationship

with temperature (Fig. 5). It is high at the inlet and the southern part of

the lagoon with a mean value of 8.5 which is similar to that of the Red


Sea water (Fig. 6). At the northern and north-eastern parts of the lagoon,

the pH decreases displaying a mean value of 8.2 (Fig. 6). It is remarkable

to see that the pH is low in the areas that are dominated by mangroves.

Fig. 5. Scatter diagram showing relationship among surface water pH, salinity (‰) and

temperature (°C) in the Shuaiba Lagoon during May 2010..

Fig. 6. Distribution pattern of surface water pH in the Shuaiba Lagoon during May 2010.

Contour interval is 0.04.


5- Water Circulation

The water column of the Shuaiba Lagoon is only 2 m thick. Based

on measurements of temperature and salinity, its structure shows two

distinctive layers, especially in the southern part of the lagoon. The

cooler (29.5° C), less saline (38‰) water of the Red Sea enters the

lagoon as surface inflow which is forced by tides and local winds

(Ahmed and Sultan, 1992; and Al-Barakati, 2010). This surface inflow

remains traceable up to the middle of the lagoon. Then, it gets more

dense and hypersaline to sink and creep on the floor of lagoon, occupying

nearly the lower 1 m of the water column (about 2 m thick) in the lagoon

(Fig. 7). It enters the Red Sea as subsurface outflow with warm and

hypersaline conditions, occupying the lower 3 m of the water column (6-

7 m thick) of the inlet/mouth (Fig. 7). Outside the lagoon, this

hypersaline subsurface outflow is still present and creeps on the floor

occupying the lower 7 m of the water column (15 m thick) at the Station

SH40 (Fig. 7). This water circulation allows renewal of the lagoon water

within 1-2 days (Al-Barakati, 2010).

Fig. 7. Distribution of salinity and temperature against depth in the water column of

Shuaiba Lagoon during May 2010 at stations SH48, SH44, SH39A and SH40. See

Fig. 1 for the location of these stations. Bottom substrates are indicated by hatched

areas.


6- Macro-Fauna and Flora

Mangrove trees are mainly of Avicennia marina dominating other

macrophytes (e.g., seagrasses, and macro-algae) in the Shuaiba Lagoon

(Fig. 8A). Mangroves occupy 10% of the total area of lagoon and are

located in tidal flat areas with water depths less than 0.2 m (Fig. 1). They

were found growing in firm, hard and soft substrates, as well as in sand-

sized, raised shoals. The soft substrate consists of black mud probably

due to decomposition of organic matter. The mangroves in the Shuaiba

Lagoon reach a maximum height of 4 m tall, occupying the areas that are

located at the intertidal-subtidal boundary to enable their

pneumatophores (aerial roots) to breathe air in habitats that have

waterlogged soil.

Seagrasses (e.g., Enhalus acoroides and Cymodocea sp.) occupy

slightly deeper environments than those of the mangroves. They are

recorded at areas of 0.5 to 1.5 m depths and having a maximum height of

35 cm (Fig. 8B, D). Their substrates vary from firm to soft. Their green

leaves are sometimes spotted by white color of larger foraminifer Sorites

orbiculus.

Many macro-algae such as: Caulerpa ethelae (sea grapes),

Caulerpa racemosa, Laurencia obtusa, Halimeda tuna (coralline alga)

and Turbinaria conoids (turbinweed) inhabit the Shuaiba Lagoon (Fig.

9). Cyanophytes (green filamentous algae) occur at the periphery of the

lagoon where the substrate is muddy. They grow forming a thick algal

mat patches at northern region of the lagoon, especially at the intertidal-

supratidal zone (sabkha) (Fig. 12D). The species Caulerpa ethelae (sea

grapes) (Fig. 9B) dominates the bottom at the middle area of the lagoon

and it is sporadically recorded in the intertidal area of the northern area.

Just before the inlet (inner inlet), the brown algae Laurencia obtuse,

Turbinaria conoids (turbinweed) (Fig. 9D, F) and the funnel weed

Padina boryana (Fig. 10A) grow more abundantly attached to hard

substrates. They proliferate also just outside the lagoon. The calcareous

green algae (Halimeda tuna) inhabit the tidal area outside the lagoon

(Fig. 9E).

Stony corals (Porites sp. and Stylophora pistillata; Fig. 11B, C)

and sponge Pericharax heteroraphis (calcareous sponge) (Fig. 11A) were

commonly found on hard substrates, immediately outside the lagoon and


close to the inner inlet. In the other parts of the lagoon, these organisms

disappear.

Fig. 8. Macrophytes from the Shuaiba Lagoon. A: the common mangrove Avicennia marina;

B: Seagrass Enhalus acoroides; C & D: Seagrasses, Cymodocea sp.

Small gastropod (Cerithidea pliculosa) and pelecypod (Mytilus

edulis) shells are the most abundant molluscs in the lagoon. They

dominate the substrates of the tidal flats of the northern part of the

lagoon. When they die, they accumulate on the shoreline, comprising a

significant part of the shore shingle (see Fig. 12B, C). At stations (SH26


and SH27), the small pelecypod Mytilus edulis is the more prolific

species, living in colonies, so their byssi intricate forming a thick mussel

mat. Large gastropod Strombus tricornis and pelecypod Tridacna sp.

shells are recorded on raised shoals at the eastern side of the lagoon.

Strombus tricornis shells are more frequent at the shoreline of the south-

eastern side of the lagoon, especially near the inlet (Fig. 11D).

Fig. 9. Macro-algae from the Shuaiba Lagoon. A: green alga; B: sea grapes Caulerpa

ethelae; C: Caulerpa racemosa; D: Laurencia obtusa; E: coralline alga, Halimeda

tuna; F: turbinweed, Turbinaria conoids.


Fig. 10. Macro-algae, hydrozoan & sponge from Shuaiba Lagoon. A: funnel weed, Padina

boryana; B: hydrozoan, Sertularella; C: sponge weed, Ceratodictyon spongiosum; D

& E: Sponge, Strepsichordaia lendenfeldi.


Fig. 11. Macro-benthos from Shuaiba Lagoon. A: calcareous sponge, Pericharax

heteroraphis; B: stony coral, Porites sp.; C: stony coral, Stylophora pistillata; D:

gastropod, Strombus tricornis.


Fig. 12. Macro-benthos & green algae from the Shuaiba Lagoon. A: a bivalve, Tridacna sp.;

B: small shells of Mytilus edulis and Cerithidea sp.; C: small shells of Cerithidea sp.;

D: dry cyanophytae (green algae).


Discussion

Shuaiba Lagoon occurs in warm, arid region and it is a shallow (~1

m depth) small basin that connected with the Red Sea water by a very

narrow passage (c. 60 m wide and 6 m deep). Thus, it is a sensitive basin

for both climatic and environmental changes. Its water physico-chemical

and biological characteristics are unique and almost different from those

of the Red Sea. The surface water temperature of the Shuaiba Lagoon

reaches 33° C during May 2010, especially in the northern part,

exceeding that of the Red Sea water by about 3° C. These conditions

make the Shuaiba Lagoon as a concentration basin, and consequently, its

surface water salinity increases to very high levels up to 60‰. This high

salinity water sinks to enter the Red Sea via the inlet as subsurface

outflow indicating an active lagoonal circulation in this small basin. This

circulation is likely to be mainly affected by density saline currents (i.e.

haline circulation). Ahmed and Sultan (1992) concluded that the

exchange of water between Shuaiba Lagoon and the Red Sea is forced by

the local winds that play a variable but sometimes dominant role in the

flushing of the lagoon, whereas tidal exchange is greatly affected by

force and direction of wind, caused by the large diurnal differences in

local heating. They also reported that seasonal mean sea level variations

do not have a significant effect on the flushing of the Shuaiba Lagoon.

In spite of occurrence of high temperature and salinity in the

northern part of the Shuaiba Lagoon that could hinder diffusion of

atmospheric CO2 into lagoon water leading to pH increase, the lowest pH

was recorded in this area. The explanation for this is that the occurrence

of high temperature in this area could enhance re-mineralization of

organic matters (mangrove litters and algal thalli) and consequently

releasing more CO2 into the waters and this leads to decrease of water

pH. This low pH could be a detrimental on the calcareous fauna (e.g.,

foraminifers and molluscs) and flora.

Prevalence of extreme temperature and salinity and low-energy,

sheltered environments in the Shuaiba Lagoon allowed, however,

occurrence of unique fauna and flora in this lagoon such as molluscs,

macro-algae, soft hydrozoans, mangroves and seagrasses. Mangroves

occur preferentially in the intertidal area of the lagoon, dominating the

intertidal zone with tall and healthy trees. In the intertidal-supratidal

zone, they are short, showing many dead branches indicating existence of


stressful environmental conditions in this area. The recorded molluscs

belong only to pelecypod species Mytilus edulis (forming shell mat in

some places) and gastropod species Cerithidea pliculosa. The Cerithidea

species is adapted to live in a wide ecological gradient from freshwater to

hypersaline and lacustrine environments and have a salinity tolerance of

3-100‰ (Plaziat 1993). Such species occur commonly in intra-

continental salt lakes (Plaziat and Younis 2005; and Abu-Zied et al.,

2011). These two species dominate the molluscs in the upper Shuaiba

Lagoon, indicating also existence of stressful environmental conditions.

Slobodkin and Sanders (1969) and Pielou (1975) mentioned that under

severe environments one or two species colonize the niches very rapidly

giving high numbers of individuals, resulting in low diversity and

causing extinction of marginal species.

Hard (aragonitic) corals are completely absent from the water of

the lagoon. They occur only around the lagoon inlet where normal Red

Sea waters predominate and optimal conditions for corals occur within

temperature of 25-30° C and salinity of 37‰ (Wright and Burchette,

1996). They also reported that in tropical and subtropical shallow water;

the temperature consistently over 20° C and salinities 32-40‰; so

carbonate producers are as calcareous green algae (Halimeda) and

hermatypic, symbiont-bearing corals that cannot tolerate high salinities,

but green algae are able to continue producing sediments.

The seagrasses (e.g., Enhalus acoroides and Cymodocea sp.),

macro-algae (e.g., Caulerpa sp., Laurencia obtuse and Turbinaria

conoids) and coralline algae dominate the bottom sediments of the

Shuaiba Lagoon where extreme temperature and salinity occur. Also,

cyanophytes (green filamentous algae) occur on the periphery of the

lagoon, forming a thick algal mat at some patches in the northern area of

the lagoon, especially at the intertidal-supratidal zone. This indicates that

these flora are able to withstand extreme high salinity and temperature.

However, persistence of such extreme environmental conditions and

dominance of these floral associations might be a resultant of prevalence

of warm, arid climatic conditions upon a small volume of water within

the Shuaiba Lagoon (Meshal, 1987). Dominance of macro-algae at the

expense of aragonitic corals in the modern sea was attributed to the

greenhouse gas-induced global warming (Hallock, 1999). We suggest

that the present environmental conditions and faunal/floral associations

of the Shuaiba Lagoon might represent a modern analogue for the


warming interval that occurred in geologic past. During Eocene,

disappearance of aragonitic corals from shallow-water carbonate

environments and dominance of coralline algae and bryozoans were used

as an indication of warming conditions accompanied with high levels of

atmospheric CO2 (Berner, 1994; and Hallock, 1999, 2001).

Conclusions

The Shuaiba Lagoon is a back-reef, shallow basin (~1 m deep)

connected with the Red Sea via a very narrow passage (about 60 m wide

and 6 m deep). It is characterized by occurrence of extreme natural

environmental conditions due to prevalence of warm, hypersaline waters

with low pH when compared with the normal Red Sea water. This warm,

high saline water goes out from the lagoon to the Red Sea as a subsurface

outflow via the deep inlet (7 m water depth). These extreme natural

conditions allowed low diverse but high abundance of calcareous macro-

fauna to occur in this lagoon. On the other hand, these conditions are

probably favorable for mangroves, seagrasses and macro-algae as

indicated by their dominance in the lagoon. Cyanophytes occur

predominately at the intertidal-supratidal zone, indicating their tolerance

to extreme high salinity and temperature. Aragonitic corals were only

observed around the inlet where normal Red Sea waters predominate.

Acknowledgement

This research was funded by the Deanship of Scientific Research,

King Abdulaziz University, Project No. 430/005-8. Early version of this

paper was read by Nuzhat Hashimi. Adel Guirguis is thanked for the

identification of macro-algae. We are also grateful to the anonymous

reviewers for their useful comments.

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New Present Environmental Status of the Shuaiba Lagoon, Red Sea … · 2011. 12. 28. · Present Environmental Status of the Shuaiba Lagoon, Red Sea Coast, Saudi Arabia 161 mainly