Ocean Colour Climate Change: Approach Identification of Sea Level

and Physical Conditions in Setokok Sea

Muhammad Zainuddin Lubis

, Wenang Anurogo

, Budiana

, Widya Rika Puspita

, Swono

Sibagariang

, Jhon Hericson Purba

, Sapto Wiratno Satoto

, Hamdani Arif

, Rahman Hakim

Hanifah Widiastuti

Budhi Agung Prasetyo

, and Husnul Kausarian

Geomatics Engineering, Politeknik Negeri Batam, Batam, Indonesia

Electrical Engineering, Politeknik Negeri Batam, Batam, Indonesia

Informatics Engineering, Politeknik Negeri Batam, Batam, Indonesia

Mechanical Engineering, Politeknik Negeri Batam, Batam, Indonesia

Marine Environmental Science, Institut Teknologi Sumatera, Lampung, Indonesia

Department of Geology Engineering, Universitas Islam Riau, Riau, Indonesia

{zainuddinlubis, wenang, budiana, widya, swono, jhonhericson, sapto, hamdaniarif, hakim, Hanifah}

Keywords: Climate Change, Sea Level, Sea Surface Temperature, Distribution of Chlorophyll A, Bathymetry.

Abstract: Setokok Island located at the South of Batam City, Riau Islands, positioned at longitude coordinates

104.031520° and latitude 0.951068°. The data acquisition technique uses satellite altimeter imagery data,

which utilizes level 3 terra fashionable satellite imagery data. The study results show a significant change

between one season (east season) with the period of data acquisition in April and May 2020. Sea surface

temperature value is 28.7

C in April 2020 and 29.8

C in May 2020. Chlorophyll A distribution has a value

of 3.5 mg/l in April 2020 and 3.2 mg/l in May 2020. The transverse profile produced by taking into account the

sea level in Setokok Sea yielding in the mean sea level height of 1.86 meters and the average sea level of 2.67

meters. These data show a significant form of bathymetry in Setokok Sea. This research shows that global

climate change affects sea level. Furthermore, it involves primary water production and bathymetry value in

Setokok Sea.

1 INTRODUCTION

Climate change is the implication of global warming.

It has resulted in conditions that are unstable in the

lower layer atmosphere, especially the layers closest

to the earth’s surface. Global warming is caused by

increasing greenhouse gases that are dominantly

caused by industries. This global warming has

increased sea surface and has affected the Chlorophyll A

distribution in the seas, especially in islands with many

industries (Collins, et al., 2010). Climate change also

by high sea levels in an area of water, especially in

Indonesia, leading to stagnant water in tidal area,

which could cause fluctuating temperatures around

the coastal environment (Susandi, Herlianti,

Tamamadin, Nurlela, 2008). Other impacts caused by

the change of sea level is coastal erosion, a decrease

in seawater salinity, higher sea surface temperature,

decreased surface water quality, and increased risk of

flooding occurring on land in coastal environments

(Oude-Essink, Van-Baaren, de-Louw, 2010). In

general, the variety of rainfall in Indonesia is strongly

influenced by its presence on the equator, monsoon

activity, the stretch of the Pacific and Indian oceans,

and highly diverse topography. Tropical cyclone

disturbances (El-Nino, La-Nina, Madden Julian

Oscillation (MJO), and hurricane winds) could also

contribute to the types of rainfall (Horhoruw,

Atmadipoera, Nanlohy, Nurjaya, 2017)

The sea level in certain area undoubtedly is related

to the depth of seawater due to the sea's physical

conditions that are in contact with each other. This

phenomenon may have an essential role in the

sustainability of human life and other living things in

coastal areas (Antoni, et al., 2019). The alteration of

coastal regions might cause shifting in seasons and

could lead to change in the pattern/distribution of

rain, which eventually might trigger floods in the

rainy season and drought in the dry season. These

Lubis, M., Anurogo, W., Budiana, ., Puspita, W., Sibagariang, S., Purba, J., Satoto, S., Arif, H., Hakim, R., Widiastuti, H., Prasetyo, B. and Kausarian, H.

Ocean Colour Climate Change: Approach Identiﬁcation of Sea Level and Physical Conditions in Setokok Sea.

DOI: 10.5220/0010351100200026

In Proceedings of the 3rd International Conference on Applied Engineering (ICAE 2020), pages 20-26

ISBN: 978-989-758-520-3

issues have always been significant problems for a lot

of islands, especially for Batam Island (Lubis, et al.,

2018). The rising sea levels might sink small islands,

cause tidal floods, and lead to storm disasters/waves

at coastal areas (Dasanto, 2010).

Setokok Sea located in the South of Batam Island,

Batam City, Riau Islands, offer alternative tourism for

beach enthusiasts to spend the weekend. In Setokok

Sea environment, there is an impact indicated by

white sand around the coast. This white sand piled up,

forming a small island, at a distance of about 4 meters

from the shoreline near the Setokok Sea. The white

dune extends to more than 10 meters and is about 3

meters wide, depending on tidal wave conditions and

sea-level values. The formation of this small land is a

phenomenon of periodical rise and fall of sea-level,

combined with the gravitational force and the

attractive force of astronomical objects, especially by

the sun, earth, and moon (Awak, Gaol, Subhan,

Madduppa, Arafat, 2016; Gaol, et al., 2015). It is

important to study the effect of climate change on sea-

level changes in Setokok Sea, which could provide

information about the physical condition of the sea by

looking at sea surface temperature values,

Chlorophyll A distribution, sea depth, and sea level.

2 RESEARCH METHODS

2.1 Research Location

This research was conducted in Setokok Sea. The

longitude and latitude coordinate is 104.031520° and

0.951068°, respectively. The area of study around 4

shown on the map in Figure 1.

2.2 Data Collection Technique

Terra Modis satellite imagery data, which is quite

well known for remote sensing, is Aqua / Terra.

MODIS (Moderate Resolution Imaging

Spectroradiometer) is an essential instrument in the

satellite Terra (EOS AM) and Aqua (EOS PM). The

MODIS Aqua / Terra satellite observes the earth's

entire surface every 1 to 2 days, obtaining data in 36

spectral band channels or groups of wavelengths

(Short, 2009; Sathyendranath, et al., 2012). MODIS

is also a satellite with a daily time series, so it is

appropriate for collecting the data (Sasmito, Parwati,

Budhiman, 2013).

Figure 1: Research location and area of study in Setokok

Sea, Batam.

In this study, data produced using recordings from

Terra MODIS satellite images for two months (April-

May 2020), with one season treatment (east season).

Additionally, data of Chlorophyll A distribution were

downloaded from https://oceancolor.gsfc.nasa.gov/.

The downloaded data was then processed by

combining them with the extracted Terra MODIS

image data. The sea surface temperature data is

obtained from extracted Terra MODIS Image data and

then classifying it for the appropriate data. These two

parameters are processed using SeaDAS and ODV

(Ocean Data View) software. Modis imagery has

three image data types, namely, Modis imagery level

1a, 1b, 2, and 3. This study uses MODIS imagery data

MODIS level 3.

2.3 Bathymetry

The bathymetry data acquisition technique is

conducted with observable data called a fixation point

with position and depth information. The bathymetry

measurements performed cannot be directly used

(processed) because it still contains data shortages

(tidal and transducer corrections) that are obtained at

the time of tidal data processing (tidal components) to

find out the actual depth appearance. The magnitude

of the tidal correction is the depth value (which has

been corrected by the transducer), which will be fixed

by the reduction value at the sea level position when

the measurement takes place. This data obtained from

the BIG Website (BATNAS)

(http://tides.big.go.id/DEMNAS/), downloaded for

two weeks in May 2020. The gridded BATNAS data

(National Bathymetry) are from 90 to 150 east

longitude and 20 southern latitudes to 20 northern

Ocean Colour Climate Change: Approach Identiﬁcation of Sea Level and Physical Conditions in Setokok Sea

latitudes. This bathymetry data has advantages in

coastal areas and shallow sea by using a survey from

the BIG Center for Marine and Coastal Environment

(PKLP) (Geospatial Information Agency).

2.4 Tidal (sea level)

Tidal data acquisition techniques obtain from the BIG

Website (Geospatial Information

Agency)

(http://tides.big.go.id/) taken based on the location

point in May 2020. In determining the water level

change in the river, there are factors such as river

hydrology, height difference, and the position of the

flow from upstream to the estuary. Near the estuary,

the water level is influenced by the sea level changes.

Data analysis is generally grouped into several

sections based on the type of data used to calculate.

The tidal data analysis is performed using Least

Square to obtain the value of tidal harmonic

constants. According to Rampengan (2009), the

classification of tidal types is carried out by

comparing the amplitudes of diurnal constants (K1

and O1) with the amplitudes of semidiurnal constants

(M2 and S2). Formzahl numbers are used to

determine the type of tides that occur in the sea

(Hidayah & Fatmawati, 2010) with a formulation

presented in Equation (1).

𝐹  𝐴𝐾1  𝐴𝑂1/𝐴𝑀2  𝐴𝑆2

(1)

Where:

F = Formzahl,

AK1 = the amplitude of the average daily single

tidal wave affected by the declination of the

moon and the sun,

AO1 = the amplitude of a single daily tidal wave

that is affected by the declination of the

moon,

AM2 = amplitude of average double daily tidal wave

children affected by the moon,

AS2 = the amplitude of the average double daily

tidal wave affected by the sun.

According to Oktavia, Pariwono, Manurung

(2011), the F value determines the characteristic of

tidal wave. The F value of 0 <F 0.25: semidiurnal;

0.25 <F 1.50: mixed tide prevailing semidiurnal; 1.50

<F 3.00: mixed tide prevailing diurnal; F> 3.0:

diurnal.

3 RESULTS AND DISCUSSION

3.1 Sea Surface Temperature

Sea surface temperature data obtained from satellite

images of fashionable terra level 3 is shown in Figure

2, with the observed location marked with the blue

box. The data for sea surface temperature is obtained

for the period of April and May 2020 (east season).

The sea surface temperature is deemed as one of the

parameters that is affected by climate change.

(A)

(B)

Figure 2: A. Sea surface temperature (April 2020), B. Sea

surface temperature (May 2020). (the data are in

ICAE 2020 - The International Conference on Applied Engineering

Figure 2 shows that the sea surface temperature is

28.7

C in April 2020 (A) and 29.8

C in May 2020

(B). These results indicate a difference in sea surface

temperature values between April and May 2020 in

Setokok Sea, with a decrease in sea surface

temperature of 0.9

C. This condition undoubtedly

affects the distribution of Chlorophyll A that occurred

in April and May 2020 (east season) due to the impact

of global climate change in 2020. The changes in sea

surface temperature due to currents, wind, water, and

waves turbidity, are commonly called ocean

dynamics. The upwelling process can also increase

Chlorophyll A content and decrease sea surface

temperature (Feng, Yao, Gu, Guo, 2007). According

to Surya, et al., (2017), sea surface temperature in

Batam is in the range of 29-31

C during January-

December period.

Figure 3 present the distribution of Chlorophyll A

is 3.5 mg/l in April 2020 (A) and 3.2 mg/l in May

2020. These results indicate a decrease of 0.3 mg/l in

the Chlorophyll A distribution in Setokok Sea. This

finding might be caused by the rising sea surface

temperature in Setokok Sea, which can decrease the

distribution of Chlorophyll A. According to Nontji

(2008), Chlorophyll A is an indicator of the

abundance of phytoplankton that becomes

zooplankton food to measure the productivity level of

primer water conditions. Hence, the decreasing

concentration of Chlorphyll A indicates the decreased

primary water productivity. Another study (Kunarso,

Hadi, Ningsih, Baskoro, 2011) has also suggested the

close relation between the Chlorophyll A levels with

the sea surface temperatures.

3.2 Tidal Analysis (sea level)

Tidal observations and measurements are made at the

coordinate of 1040 1 '50 " - 1040 2"35 " east longitude

and 00 56"35" - 00 57"32" north latitude. The sea in

Setokok tend to be double tilt or semi-diurnal (mixed

tide prevailing semi- diurnal), meaning that there are

two tides in a day, but the two pairs are not as large as

the tidal graphs shown in Figure 4.

The tidal component analysis is performed to

obtain the value of each tidal component's amplitude

and bead phase. The method used is the Least Square.

After the analysis is carried out, the constant

harmonic values obtained are presented in the Table

(A)

(B)

Figure 3: A. Chlorophyll A distribution (April 2020), B.

Chlorophyll A distribution (May 2020).

Figure 4: Tidal wave chart (May 20, 2020).

Table 1: The value of amplitude (A) and phase (G) of the

harmonic constants of tidal wave studied.

Componen

M2 S2 N2 K2

Value

0.3527 0.3884 0.0731 0.3332

Componen

O1 P1 M4 MS4

Value

0.2673 0.1819 0.0112 0.0038

Ocean Colour Climate Change: Approach Identiﬁcation of Sea Level and Physical Conditions in Setokok Sea

The data are taken in the second half of the month

in May 2020, where the moon's condition was convex

at the end of the month to the end of the month, or it

could be called a crescent. By entering these constant

values into the Formzahl number equation, an amount

of 0.81 will obtain. Based on this number, the type of

mixed tides tends to be Semidiurnal. It means that

there are two pairs of waves and two times receding

with different heights and periods in one day. The

dominant tidal components based on the above

calculation are the S2 and M2 component with an

amplitude value of 0.3884 and 0.3527, respectively. In

contrast, the non-dominant tidal element in MS4 with

an amplitude value of 0.0038 proves that the regional

tidal type is a mixed type. The amount of retroactivity

is influenced by intense sun penetration that affects

the sea surface temperature due to climate change

(Adibrata, 2007). By using the Least Square method,

the results obtained from tidal harmonic analysis are

harmonic components that can be used to determine

sea level elevation values. The results of sea-level

elevation in Setokok coastal seawater are:

 Mean High Water Level during the observation

period is 1,860 meters.

 Mean Sea Level, which is the mean water level

between the mean high water level and the mean

low water level. This elevation using as a

reference for elevation on land is 2,675 meters.

 Mean Low Water Level is the lowest water

level at high tide.

According to Suhelmi (2013), the sea-level values

shows that the increase in tidal inundation area due to

sea-level rise plays a significant role in the amount of

vulnerability index. This is due to the relationship to

global climate change that occurs in water. Sea

surface anomalies are strongly influenced by tides,

topography, wind, ocean currents, density, and

seawater pressure, especially in Setokok Sea.

3.3 Cross-profile and Water

Bathymetry

The water cross-section profile shows a cross-section

of one of the samples in the area's coastal part, with a

relatively steep to the sloping surface. In Figure 5, it

can be seen that the height of the coastal surface

decreases as it heads towards the coast.

From Figure 5, the results of three samples taken in

the form of a cross-section, wherein example 1

illustrates that the surface is relatively steep in the

northern part of the study area and the southern part of

the study area. Whereas in samples 2 and 3, the site's

bottom surface looks slightly sloping compared to

sample 1. The 3-dimensional and 2- dimensional form

of bathymetry for the area of study of the water bottom

is shown in Figure 6.

The condition of the bathymetry of the sea in the

location indicates that the location is suitable for a

port and its support. The ship sailing activities

generally

requires water depth that is equal to the

ship's requirements (draft) plus different depth. Based

on the data observed, this water area is eligible for

shipping activities. The depth of the

port/pier/terminal water is usually determined from

the size of ships that are frequently entering the dock.

The giant ship that rarely comes could only enter the

port when the sea is in high tide. The depth of the ocean

around Batam Island is already mapped by BATNAS

BIG, which divided the area into four depth levels,

namely depth of 1-5 meters, 5-10 meters, 10-20

meters, and> 20 meters. Sea with the depth of 1-5

meters locates around the coast and spread throughout

Batam City. For the depth of 5-10 meters, categorized as

inter-island sea belong to the Regency of Batam and

other areas. The area with the depth of 1-5 meters are

included in the development of the coastal regions

while the area with the depth of 5-10 meters is

intended for shallow sea areas. The area with the

depth of 10-20 meters and >20 meters is for the

development of deep-sea areas.

Figure 5: The cross-sectional profile of Setokok Sea.

ICAE 2020 - The International Conference on Applied Engineering

(A)

(B)

Figure 6: Bathymetry of Setokok Sea (A) 2 dimensions, and

(B) 3 dimensions

Setokok Sea is part of the shallow area with the

depth distribution ranging from 0 to 16 meters below

sea surface. The deepest point locates at a distance of

16 m to the northeast while the lowest depth (0-5

meters) can be placed around the Setokok beach.

Setokok Sea has a relatively steep surface in the north

and south. On the east, the sea floor looks more

gentle. As for the coastal areas of Setokok, the surface

is relatively steep until the sloping height of the

coastal surface decreases as it heads towards the

coast. Thus, it can be seen that the sea level's value

must have a significant effect on the steepness of the

bathymetry in an area of water, especially in seawater

like Setokok. Hasan (2004) studied that other

important factors that can influence climate change

are the average topography and the value of the depth

of the ocean in water.

4 CONCLUSIONS

From the results of research conducted in one season,

it can show the difference in sea surface temperature

and the distribution of Chlorophyll A in April and May

2020 (east season). The higher the sea surface

temperature, the lower the Chlorophyll A's

distribution value in Setokok Sea. This is also related

to the sea level that changes every day, and

dramatically affects the bathymetry and steepness of

the transverse profile in Setokok Sea. The results

show climate change observed from the parameters

studied, namely the sea surface temperature, the

distribution of Chlorophyll A, tides (sea level), cross

profile, and bathymetry values. The change of those

parameters caused by global climate chage tend to

affect the primary water condition in Setokok Sea

Batam islands.

ACKNOWLEDGEMENTS

The authors thank Politeknik Negeri Batam for

facilitating this research by providing research grant

funds in the middle of research schemes (DIPA funds

in 2020).

REFERENCES

Adibrata, S., 2007. Analisis pasang surut di Pulau

Karampuang, Provinsi Sulawesi Barat. Akuatik: Jurnal

Sumberdaya Perairan, 1(1), 1-6.

Antoni, S., Bantan, R. A., Al-Dubai, T. A., Lubis, M. Z.,

Anurogo, W., Silaban, R. D., 2019. Chlorophyll A, and

Sea Surface Temperature (SST) as proxies for climate

changes: case study in Batu Ampar waters, Riau

Islands. In IOP Conference Series: Earth and

Environmental Science (Vol. 273, No. 1, p. 012012).

IOP Publishing.

Awak, D. S., Gaol, J. L., Subhan, B., Madduppa, H. H.,

Arafat, D., 2016. Coral reef ecosystem monitoring

using remote sensing data: case study in Owi Island,

Biak, Papua. Procedia Environmental Sciences, 33,

600-606.

Collins, M., An, S. I., Cai, W., Ganachaud, A., Guilyardi,

E., Jin, F. F., Vecchi, G., 2010. The impact of global

warming on the tropical Pacific Ocean and El Niño.

Nature Geoscience, 3(6), 391-397.

Dasanto, B. D., 2010. Penilaian dampak kenaikan muka air

laut pada wilayah pantai: Studi kasus Kabupaten

Indramayu. Jurnal Hidrosfir Indonesia, 5(2).

Feng, J., Yao, Z., Gu, M., Guo, H., 2007. The climate

change and its ecosystem effect in the upper yellow

river. In 2007 IEEE International Geoscience and

Remote Sensing Symposium (pp. 793- 796). IEEE.

Gaol, J. L., Leben, R. R., Vignudelli, S., Mahapatra, K.,

Okada, Y., Nababan, B., Syahdan, M., 2015. Variability

of satellite-derived sea surface height anomaly, and its

relationship with Bigeye tuna (Thunnus obesus) catch

in the Eastern Indian Ocean. European Journal of

Remote Sensing, 48(1), 465-477.

Ocean Colour Climate Change: Approach Identiﬁcation of Sea Level and Physical Conditions in Setokok Sea

Hasan, S., 2004. Kepadatan dan pola distribusi

echinodermata di zona intertidal pantai pulau Ternate.

Media Ilmiah MIPA, 1(1), 1-9.

Hidayah, Z., Mahatmawati, A. D., 2010. Perbandingan

fluktuasi muka air laut rerata (MLR) di perairan pantai

utara Jawa Timur dengan perairan pantai selatan Jawa

Timur. Jurnal Kelautan: Indonesian Journal of Marine

Science and Technology, 3(2), 159-167.

Horhoruw, S. M., Atmadipoera, A. S., Nanlohy, P.,

Nurjaya, I. W., 2017. Anomaly of surface circulation

and Ekman transport in Banda Sea during ‘Normal’and

ENSO episode (2008-2011). In IOP Conference Series:

Earth and Environmental Science (Vol. 54, No. 1, p.

012041). IOP Publishing.

Kunarso, K., Hadi, S., Ningsih, N. S., Baskoro, M. S., 2011.

Variabilitas suhu dan klorofil-a di daerah upwelling

pada variasi kejadian ENSO dan IOD di perairan

selatan Jawa sampai Timor. ILMU KELAUTAN:

Indonesian Journal of Marine Sciences, 16(3), 171-

180.

Lubis, M. Z., Anurogo, W., Mufida, M. A., Taki, H. M.,

Antoni, S., Lubis, R. A., 2018. Physical condition of the

ocean to global climate change variability: case study

in the Batam waters, Indonesia. In 2018 International

Conference on Applied Engineering (ICAE) (pp. 1-4).

IEEE.

Nontji, A., 2008. Plankton laut, Yayasan Obor Indonesia.

Jakarta.

Oktavia, R., Pariwono, J. I., Manurung, P., 2011. Variasi

muka laut dan arus geostrofik permukaan perairan Selat

Sunda berdasarkan data pasut dan angin tahun 2008.

Jurnal Ilmu dan Teknologi Kelautan Tropis, 3(2), 127-

152.

Oude-Essink, G. H. P., Van-Baaren, E. S., de-Louw, P. G.

B., 2010. Effects of climate change on coastal

groundwater systems: A modeling study in the

Netherlands. Water resources research, 46(10).

Rampengan, R. M., 2009. Pengaruh pasang surut pada

pergerakan arus permukaan di Teluk Manado. Jurnal

Perikanan dan Kelautan Tropis, (3), 15-19.

Sasmito, B., Parwati, E., Budhiman, S., 2013. Analisis

distribusi total suspended matter dan Klorofil-a

menggunakan citra terra modis level 1b resolusi 250

meter dan 500 meter (studi kasus daerah pesisir

Kabupaten Pesawaran Provinsi Lampung tahun 2012).

Jurnal Geodesi Undip, 2(1).

Sathyendranath, S., Brewin, B., Mueller, D., Doerffer, R.,

Krasemann, H., Mélin, F., Steinmetz, F., 2012. Ocean

colour climate change initiative—Approach and initial

results. In 2012 IEEE International Geoscience and

Remote Sensing Symposium (pp. 2024- 2027). IEEE.

Short, N. M., 2009. The remote sensing tutorial: the

concept of remote sensing. Retrieved March 23

, 2020,

from

http://geoinfo.amu.edu.pl/wpk/rst/rst/Front/overview.h

tml

Suhelmi, I. R., 2013. Pemetaan kapasitas adaptif wilayah

pesisir Semarang dalam menghadapi genangan akibat

kenaikan muka air laut dan perubahan iklim. Forum

Geografi, 27 (1), pp. 81-92.

Surya, G., Khoirunnisa, H., Lubis, M. Z., Anurogo, W.,

Hanafi, A., Rizky, F., Mandala, G. F. T., 201).

Karakteristik suhu permukaan laut dan kecepatan angin

di perairan batam hubungannya dengan Indian Ocean

Dipole (IOD). Dinamika Maritim, 6(1), 1-6.

Susandi, A., Herlianti, I., Tamamadin, M., Nurlela, I., 2008.

Dampak perubahan iklim terhadap ketinggian muka

laut di wilayah Banjarmasin. Jurnal ekonomi

lingkungan, 12(2).

ICAE 2020 - The International Conference on Applied Engineering