Journal of the Persian Gulf
(Marine Science)/Vol. 5/No. 18/December 2014/12/37-48
Study of the Physical Oceanographic Properties of the
Persian Gulf, Strait of Hormuz and Gulf of Oman
Based on PG-GOOS CTD Measurements
Azizpour, Jafar*; Chegini, Vahid; Khosravi, Maziar; Einali, Abbas
Iranian National Institute for Oceanography and Atmospheric Science, Tehran, IR Iran
Received: June 2014
. Accepted: November 2014
© 2014 Journal of the Persian Gulf. All rights reserved.
Abstract
The present study covers the results from the CTD observations of the PG-GOOS cruises. CTD profiles
were collected in eight cruises at 169 stations, from fall 2012 to the late summer 2013. Spatial and
temporal distributions of the temperature, salinity and density were investigated. In summer, water column
at deep stations was strongly stratified and at shallow stations water column was moderately well-mixed.
The coincidence of surface heating resulted in the strength of summer stratification. Increasing in
temperature and particularly salinity near the bottom in southern stations of the Strait of Hormuz indicated
trace of the Persian Gulf Water outflow. Strong and weak thermocline layers are formed in summer
(∆
12 ) and winter in deep stations (∆
6 ), respectively. T-S diagrams at deep part of the Strait
of Hormuz showed two water masses i.e. the Indian Ocean Surface Water (IOSW) inflow to the Persian
Gulf and Persian Gulf outflow dense water. The movement of scatter plots along temperature and salinity
axes indicated the influence of the seasonal variations of the Indian Ocean Surface Water (IOSW). The
results of this project are the most historically magnificent oceanographic survey of the Persian Gulf and
Gulf of Oman with wide range of applications.
Keywords: Persian Gulf, Strait of Hormuz, Gulf of Oman, PG-GOOS, Physical Oceanography, Hydrography.
1. Introduction
of Hormuz, and the Gulf of Oman is one of the most
political and economical waterways in the world
(Fig. 1). The Persian Gulf (a shallow semi-enclosed
basin) is a very important piece of world’s ocean
water because of its rich gas and oil sources. The
Straits of Hormuz which is only 56 km wide at its
narrowest point, connects the Persian Gulf with the
Gulf of Oman and the northwestern part of the Indian
Ocean. Despite of limited and sparse investigations
in the coastal waters to the best of our knowledge, a
few basin-wide oceanographic surveys have been
I.R. Iran is situated along 5700 kilometer of
coastlines of the Persian Gulf, the Strait of Hormuz,
and the Gulf of Oman in the South as well as the
Caspian Sea in the North. Oceanographic and marine
studies, bearing in mind the geographical, political,
and economic situation of the I.R. of Iran, depend on
collecting information and data. Without doubt, the
oceanic region including the Persian Gulf, the Strait
*
Email: [email protected]
37
Azizpour et al.
a / Study of thhe Physical Oceanographic
O
c Properties of the Persian Gulf, Strait…
Reyn
nolds (1993) reported the fifirst compreh
hensive set off
CTD
D measuremen
nts, current m
meter moorin
ng data, buoyy
track
king, and obsservation of m
many meteorrological dataa
in th
he Persian Gu
ulf. The survvey continued
d for about 4
montths, covering
g the period oof February to June 1992..
Wateer propertiess measurem
ment did nott cover thee
shalllow shelf of the southernn Persian Gulf. Swift andd
Bow
wer (2003) explained
e
the
he aspects of
o the waterr
properties in thee Persian G
Gulf by usin
ng availablee
hydrrographic dataa from Januaary to Augusst. Moreover,,
the Regional
R
Organization fo
for the Proteection of thee
Mariine Environm
ment (ROPME
E) also condu
ucted severall
basin
n-wide survey
ys in the Perrsian Gulf du
uring summerr
of 20
000 and 2001 and winter oof 2006.
don
ne in this reegion (Reynoolds, 1993). Regional annd
loccal oceanoggraphic dataa collected via vessells,
sattellites or othher means are
a sources of
o informatioon
to develop apppropriate moddels for objeective-orienteed
goals in marinee ecosystemss.
Regional coountries havee investigated
d their coasttal
he scope of th
the
waaters which inn the in the Peersian Gulf, th
datta is limited to temporall and spatial coverage annd
onlly a few baasin-wide surrvey results are publisheed.
Temperature-saalinity data was publish
hed by Emeery
(19
956) from tthe Germann ship Meteeor expeditioon
cov
vering the 19948 summerr cruise. Lateer, Brewer annd
Dy
yrssen (1984)) reported a wintertime survey of th
the
Atllantis from W
Woods Hole Oceanograp
phic Institutioon.
Fig. 1: Map of the Persian
P
Gulf, th
he Strait of Horm
muz and the Gu
ulf of Oman, CT
TD casts. Boxees show the eigh
ht
crruise study areaa. In Box 2, cru
uise was done inn 2 seasons (2 times) and in Bo
ox 3 cruise repeeated 3 times.
38
Journal of the Persian Gulf (Marine Science)/Vol .5/No .18/December 2014/12/37-48
the Persian Gulf is reported about 35.3 to 110 Km3/yr
(Chao, et al., 1992; Reynolds, 1993).The most
significant weather phenomenon in the Persian Gulf is
northwesterly Shamal wind, which occurs during the
year (Perrone, 1981). Winds in the Gulf of Oman are
influenced by the Indian Ocean monsoon system,
reversed seasonally between northwest southeast in
winter and summer, respectively (Reynolds, 1993).
The Iranian National Institute for Oceanography
and Atmospheric Science (INIOAS) performed the
“Persian Gulf and Gulf of Oman Oceanographic
Study” (PG-GOOS) project in an interdisciplinary
format. This project is the longest Oceanographic
field operation in the Persian Gulf and Gulf of Oman
that commenced on November 5, 2012 and was
continued for one year (Table 1). As far as we are
aware of, there is no previous survey to cover the
area during four seasons.
2.2. Field Measurements
Table 1. List of Observational Cruises for Oceanographic
data collection
Cruises
Date
PG-GOOS 1
PG-GOOS 2
PG-GOOS 3
PG-GOOS 4
16-30/11/2012
19-25/12/2012
27/1-1/2- 2013
17-22/2/2013
Number of
Stations
26
17
24
16
PG-GOOS 5
2-4/3/2013
11
PG-GOOS 6
PG-GOOS 7
PG-GOOS 8
2-6/5/2013
28-31/7/2013
13-21/8/2013
15
29
31
Vertical profiles of the conductivity, temperature and
pressure were measured at 169 stations that covered the
Persian Gulf, Strait of Hormuz and off Chabahar Bay in
the Gulf of Oman (Fig. 1), using a multi-parameter
CTD probe, at 8 multidisciplinary cruises from fall
2012 to the late summer 2013 (Table 1). CTD casts
were performed using an Ocean Seven 316, Idronaut,
mounted on a 12-bottle Rosette equipped with the pH,
chlorophyll-a, turbidity and dissolved oxygen sensors.
The accuracy of the temperature and conductivity
sensors were 0.003°C and 0.003 mScm
with a
resolution of 0.0005°C and 0.001mScm ,
respectively (Idronaut, 2002). Before the cruise, the
CTDs probe were calibrated, cross checked and also set
to the timed data acquisition mode with a 1 second time
step. The CTD lowered into the water columns with a
constant speed of 1ms during the different casts. To
avoid turbulence caused by the rosette package on the
up casts, the present study employed those down casts
data obtained through different CTD casts.
Finally, all vertical profiles were low-pass filtered
with a cut-off length of 5 m, and ordered of 4 to
suppress the high-frequency noises, and also to avoid
aliasing errors (Wieczorek et al., 2008).
Location
East Part of PG
West Part of PG
Hormuz Strait
Gulf of Oman
From Hormuz
Strait to Jask
Hormuz Strait
Hormuz Strait
East Part of PG
2. Materials and Methods
2.1. Study Area
The study area is located in the Iranian part of the
Persian Gulf (PG), Strait of Hormuz, and the Gulf of
Oman (Fig. 1). The stations were selected based on
the bathymetric contours and other disciplines to
cover some specific depth within the mention area.
The Persian Gulf is about 990 km long and has a
maximum width of 370 km between Iran and U. A. E.
The average depth of the Persian Gulf is 36m and it
occupies a surface area of about 239, 000 km2 (Emery,
1956). The Persian Gulf is located between latitudes
24-30°N that is exposed to arid, sub-tropical climate
(boundary of the tropical and mid-latitude weather
systems) due to southern deserts, which surrounded it.
The seasonal shifting of the tropical and mid-latitude
systems leads to seasonal changes in the meteorological
conditions (Reynolds, 1993). The evaporation rate is
variable and fluctuates between 1.4 and 5.0 m/yr
(Privett, 1959; Meshal and Hassan, 1986; Ross and
Stoffers, 1978; Johns et al., 2003). The total run off to
3. Results
3.1. Spatial and Temporal Variations of the
Temperature, Salinity and Potential Density
The locations of measurements during the first
39
Azizpour et al. / Study of the Physical Oceanographic Properties of the Persian Gulf, Strait…
Gulf, both temperature and salinity increased in two
seasons and core of the warm and salty water located
between 53-54 °E. Cold and low saline water of the
Gulf of Oman went through at the Iranian Part of the
Persian Gulf and developed in the Persian Gulf. The
length of the mentioned inflow development
depended on the wind speed (Reynolds, 1993).
and eighth cruises in the east part of the Persian Gulf
are shown in Box 2, Figure 1. In November, surface
temperature and salinity; changed from 26.8 to 28.5
°C and 36.2 to 39.5 psu, respectively. Alternatively,
in August, temperature varied from 29.0 to 34.1 °C,
and salinity changed from 36.9 to 39.1 psu (Figures
2I, II). From the Strait of Hormuz to the Persian
I
NOVEMBER
Temperature (Surface Layer)
27.7
IRAN
28
28
27.4
26.6
27.7
26.4
27.5
27.7
9
28
26
27.5
26.
N
26.2
27.2
28
27.
9
26.8
27
27.5
27
28.2
Latitude (degree)
27.2
28.3
25.8
Salinity (Surface Layer)
.9
.9
37
.6
36.6
37
.4
26.6
37
.3
38.5
.6
36
26.4
38.7
26
36.6
39.4
26.2
37.9
Latitude (degree)
38
.7
38
26.8
38.9
39.1
27
38
37
38
27.2
25.8
52.5
53
53.5
54
54.5
55
55.5
56
Longitude (degree)
II
AUGUST
Temperature (Surface Layer)
IRAN
33.5
26.2
33
.5
.75
N
26
33.25
25.8
.75
32
3
33
31.7
29.5
26.4
33
5
3.2
30.5
33.5
26.6
31
26.8
32.25
27
34
Latitude (degree)
27.2
29
31
.5
5
33.7
5
Salinity (Surface Layer)
37.15
37.9
37.4
4
37.
38.9
26.6
26.4
37.9
38.
4
26
38.4
26.2
38.9
38.15
25.8
52.5
53
53.5
37.15
26.8
37.9
37
.65
38.15
27
.65
38
Latitude (degree)
27.2
54
54.5
55
55.5
56
Longitude (degree)
Fig. 2: Horizontal distribution of surface temperature and salinity for; I: first and II: eighth cruise in east part of the Persian Gulf.
40
Journal of the Persian Gulf (Marine Science)/Vol .5/No .18/December 2014/12/37-48
CTD casts in the first and final cruises and was in
agreement with previous studies (e.g. Reynolds, 1993;
Yao, 2008). Comparing of salinity contours (Figures 2
I, II) showed that the Persian Gulf surface waters were
more saline in November and near the Strait of Hormuz
in August. In summer, the salinity of the IOSW layer
increased to ~ 37.9 psu, and the surface temperature
raised to abou 30°C. However, the November cruise
showed that the salinity and the temperature of IOSW
were 37 psu and lower than 27.5°C, respectively. In
November, the length of mixing layer expanded from
the surface to ~ 50 m (Figure 3a) and whole water
column was well mixed near the coastal zone and also
near the islands, while in August (Figure 3b) its length
decreased to ~ 20 m. Under mixed layer, weak
thermocline (∆t~6
layer appeared and expanded to
~ 70 m in the early fall.
The surface inflow of Indian Ocean Surface Waters
(IOSW) in winter was warmer than the Persian Gulf
waters (Fig. 2), and as it advected into the Persian Gulf,
the IOSW underwent the surface cooling (longitude ~
55°E) and IOSW overlaid the Persian Gulf surface cold
water (Fig. 6 II). Density variations (not shown here)
showed penetrations of the low saline IOSW in the
western part of the Strait of Hormuz and in the east part
of the Persian Gulf that, expansions of IOSW were
changed seasonally, i.e. it was expanded deeper in the
Persian Gulf during summer in contrast to winter. On
the other hand, density differences were affected by the
low saline IOSW in the cold seasons, while both
salinity and temperature affected the density changes in
the winter time. Density increased from the Strait of
Hormuz to the head of the Persian Gulf all year round,
which was confirmed through Figures of the
Fig. 3: Vertical profiles of temperature, salinity and sigma-t for some selected deep stations in a: November, b: August.
41
Azizpour et al.
a / Study of thhe Physical Oceanographic
O
c Properties of the Persian Gulf, Strait…
Moreover, during midddle of su
ummer stronng
theermocline (∆t~12
waas even geneerated betweeen
20 and 60 m. N
Naturally, beellow the therrmocline layeer,
thee temperaturee, salinity annd sigma-t did not changge,
and
d the data shoowed the sam
me results and
d consequenttly
waater column w
was well mixeed. Overall variation
v
rangges
of the temperaature, salinityy and densitty were, 20..528.7 , 36.38- 40.8 psu and
a 23.7-29.35 Kg⁄m in
No
ovember and also were 20.9-33.3
2
, 36.9- 40.8 ppsu
⁄
and
d 22.5- 29.655 Kg m in August,
A
respectively.
Contours oof the spaatial variations of thhe
tem
mperature, saalinity and deensity, along the transect II
(Bo
ox 1 in Fig. 1) of the PG
G-GOOS seccond cruise aare
sho
own in Figurre 4.
There are tw
wo weak temperature fronts
fr
betweeen
staations 2 andd 5. Verticaal patterns of
o temperatuure
weere uniform
m between stations 11 and 114.
Distrribution of the density was similarr to that off
salin
nity owing to
t winter deensity chang
ges initiatedd
prim
marily by chaange in salinnity. High-density waterr
existted in lower layer betweeen the stations 2 and 8
and particularly bottom paart of the station
s
5. Itt
soun
nds that in offfshore, the m
main reason for changess
of potential
p
den
nsity was saalinity chang
ges while inn
near shore, both
h salinity annd temperatu
ure changess
affeccted potentiaal density aalterations (F
Figs 4I, II)..
Denssity (salinity
y) front betw
ween station
ns 11 and 8
appeeared to beend towardds station 8 which itt
exten
nsion to the sea surface could not be
b confirmedd
(only
y expands to
t ~ 20 m, Figure 4I). Tongue off
Salin
ne and warm
m water expannded in uppeer layer from
m
the offshore
o
statiions to coasttal zone and
d in contrast,,
low--salinity and low-temperaature water tongue
t
couldd
be ob
bserved in th
he lower layeer (Fig. 4II).
Fig. 4: Verttical distribution
n of temperaturre, salinity, and
d potential densiity in cross shellf (I) and
along out line of
o observations (II) of second C
Cruise (PG-GO
OOS II), see Fig
gure 1 left side ffor positions
42
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Figures 55I, II show, vertical
v
sections of temperrature,
he Persian G
Gulf Water (P
PGW). Vertical
outflow of th
salinity and density alonng and cross the Hormuz strait
variations of both temperaature and salinity suggessted
axis (Box 4 Fig. 1, cruuises 5). Tem
mperature, saalinity
sttrong stratification betweeen stations 6-11 bellow
w 40
°
and density changed froom 22.5 to 24
4.0 C 36.4 too 39.3
m (Fig. 5I) and moderate m
mixed layer between
b
statiions
⁄m , respecttively. From
psu and 24.7 to 27.8Kg⁄
m ~ 90
3 and 6. Th
hese conditioons observed in the crross
m to bed, a considerabble increase of salinity ((37.9-
seection transeect (Fig. 5II)) except for the lower laayer
°
39.3) and temperaturee (26.5-27.8 C) indicateed to
(b
bellow 90 m)) that fairly w
was well mixeed.
Fiig. 5: Vertical seections of temp
perature (upper)), salinity (midd
dle) and density
y (lower) along strait axis (I) between
S
Sts. 3, 6, 9 and 11, and cross sttrait axis (II) beetween Sts. 7, 8 and 9. Position
ns of Sts. shownn on Box 4, Fig
gure 1
43
Azizpour et al.
a / Study of thhe Physical Oceanographic
O
c Properties of the Persian Gulf, Strait…
Figures 6I, III, III, and IV
V show verticcal distributioon
of the temperatture, the saliinity and the density in th
the
Strrait of Hormuuz (Box 3, Fig.
F 1, cruisee 3). At path I,
waater column w
was strongly stratified an
nd only a weaak
fro
ont could be find bellow 60 m betweeen Stations 221
and
d 22. The colld cores weree traceable in
n ~ 50 m deppth
at Stations 17 aand 24, and thhese cores weere PGW lyinng
belllow Indian Ocean surfacce warm waater (Fig. 6 III).
Beetween two mentioned cores, waterr column w
was
hom
mogenous.
Some part oof other cold core was tan
ngible betweeen
staations 9 and 10, which it saank and makee a temperatuure
fro
ont bellow 550 m betweeen stations 13
1 and 6. Thhe
Perrsian Gulf saalty water saank in deep part
p of statioons
betw
ween 24 and 19
1 and it laidd bellow the Indian
I
Oceann
dens water. Wheen slightly lless dense of
o the Indiann
Oceaan Water (th
he compare with the Persian
P
Gulff
outfllow dense waters)
w
and th
the Persian Gulf
G outflow
w
dense waters gett together, th
the Indian Ocean
O
waterss
ascen
nded (Fig. 6II, between stations 17 and 19) andd
overllaid the Perrsian Gulf ooutflow watters. Densityy
variaations conform
med salinity variations co
ompletely. Att
path III the temp
perature and the salinity variations inn
wateer column weere ~1 , an
and 0.3 psu, respectively..
Wateer column was
w stronglyy stratified. At
A path IV,,
bello
ow 50m depth,
d
the temperaturee increasedd
remaarkably betweeen stations 8 and 9. In th
his layer, thee
salin
nity increased to 38.6 psu.
Fig. 6-1: Vertical seections of tempeerature (upper), salinity (middle) and density (low
wer) west part off Hormuz strait inn cross strait axis (I), along straitt
axiss (II), in middle ppart of strait crosss strait axis (III) and in east part oof strait cross straait axis (IV). Possitions of Sts. shoown on Box 3, Figure 1.
44
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Fig. 6-2: Verticcal sections of tem
mperature (uppeer), salinity (midddle) and density (lower) west parrt of Hormuz strrait in cross straitt axis (I), along strait
s
axis (II), in midddle part of strait cross strait axis (III)
( and in east ppart of strait crosss strait axis (IV).. Positions of Stss. shown on Box 3, Figure 1.
3.2. T-S Diaagrams
other hand, due to poossibility off high rate of
ev
vaporation in summer ttime, deeperr inflow of the
Figure 7 shows T-S diagrams
d
for the Persian Gulf,
IO
OSW into th
he Persian G
Gulf was reesulted. Duee to
Strait of Hoormuz and the Gulf of Om
man of PG-G
GOOS
sttrong thermo
ocline layer inn deeper stattions (out of the
cruises. Figuures 7A andd F illustrate T-S diagram
ms for
sttrait), water column
c
was strongly straatified. This was
w
the eastern section of thhe Persian Gulf
G during w
winter
ev
vident from
m heating att the sea surface
s
and in
and summeer, respectiveely (Box 2 in
i Fig. 1). A
At the
ag
greement wiith previous observationss (Alessi et al.,
western secction of the Strait
S
of Horm
muz variatioons of
1999; Bower et al., 2000; Reynolds, 19
993). Moreovver,
the temperature, saliniity and poteential densitty in
movement
m
off scatter ploots along teemperature and
winter and summer tim
me were, 4, 3.5°C (27.5--31.5,
saalinity axes was
w an evidennce of season
nal variations in
24-27.5), 2.00, 0.5 psu (37-39, 36.5-37
7) and 3.0 annd 1.0
IO
OSW penetraation (Figs 7A
A and F). Figures 7C andd D
Kg⁄m (222.8-25.8, 24.1-25.1), resp
pectively. Onn the
sh
how two lay
yers in the Sttrait of Horm
muz. At Irannian
45
Azizpour et al.
a / Study of thhe Physical Oceanographic
O
c Properties of the Persian Gulf, Strait…
sid
de of strait, water colum
mn was hom
mogeneous in
ut 36.5 psu.. In this laayer, water temperaturee
abou
shaallow stationns. In deep stations at the Strait of
decreased to ~ 22
2
Ho
ormuz, wateer column was consissting of tw
wo
temp
perature waas rather
lay
yers, e.g. suurface layer with ~ con
nstant saliniity
increeased about 3 psu.
(Fig. 77D). At loweer layer, thee
constant, but
b
salinityy
Fig
g. 7: T-S diagram
ms: (A) first cruuise of PG-GOOS (East part oof PG, winter time), (B) second
d cruise of PG--GOOS (West part
p of PG), (C))
Easst part of Horm
muz Strait to Jask, (D) Strait off Hormuz, (E) G
Gulf of Oman, off
o Chabahar Bay, and (F) Eigghts cruise of PG-GOOS (Eastt
parrt of PG, summeer time), see Figgure 1 for locattions.
46
Journal of the Persian Gulf (Marine Science)/Vol .5/No .18/December 2014/12/37-48
4. Discussion
References
The CTD observations in the PG-GOOS cruises
were carried out to elucidate the distribution of
temperature, salinity and water column stratification.
Penetrations of the IOSW depend on evaporation rate
and northwest wind speed (Reynolds, 1993). Results
of salinity contours showed that influence of the
IOSW in the summer was wide spreading and
extended to the north head of the Persian Gulf. While
in the winter, influences of IOSW were limited due
to force of northwesterly wind. Density contours of
second cruise (not shown here) revealed one of dense
water source in the northern end of the Persian Gulf,
which was reported in earlier studies (see e.g. Swift
and Bower, 2003; Yao, 2008; Yao and Johns, 2010).
Mixed layer thickness increased in winter time and
reached to ~ 50 m. Due to surface heating in summer
time, mixed layer thickness got to 20 m in ultimate
conditions. Alternatively, thickness of thermocline
layer increased to ~ 40 m in hot season and in cold
time, it was relatively absent in the Persian Gulf.
There was a reasonable relationship between
thermocline and halocline layer in water column. The
temperature and the salinity vertical section contours
in eastern section of the Strait of Hormuz revealed
that inflow water volume in August was much
greater than in November, which could be because of
high evaporation rate and low river inflow in
summer. In majority of stations, when temperature
decreased with depth sharply, salinity increased
sharply, except in cases with intrusion of different
water mass. Temporal and spatial distributions of
water masses, were different in the study area. In the
Persian Gulf region, whole water column was mixed
in winter and consequently there was only one water
mass while with changing season to the summer, two
water masses were demonstrable, especially in deep
stations. In the Strait of Hormuz, there were two
water masses throughout the year. Finally, three
water masses is common in deep stations in the Gulf
of Oman.
Alessi, C. A., H. D. Hunt and A. S. Bower,
1999. Hydrographic data from the US Naval
Oceanographic Office: Persian Gulf, Southern Red
Sea, and Arabian Sea 1923–1996, Woods Hole
Oceanog. Inst. Tech. Rep., WHOI-99-02, 74P.
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Brewer, P. G. and Dyrssen, D., 1985. Chemical
Oceanography of the Persian Gulf, Progress in
Oceanography, 14: 41–55.
Chao, S. Y., Kao, T. W., and Al-Hajri, K. R., 1992.
A numerical investigation of circulation in the
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Emery, K. O., 1956. Sediments and water of Persian
Gulf. American
Association
of
Petroleum
Geologists Bulletin, 40(10): 2354-2383.
Idronaut, 2002. Ocean seven 316/319 CTD
multiparameter probes operation’s manual, Idronaut,
Brugherio, 145P. http://www.idronaut.it.
Johns, W. E., Yao, F., Olson, D. B., Josey, S. A.,
Grist, J. P. and Smeed, D. A., 2003. Observations
of seasonal exchange through the Straits of
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