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Friday, February 1, 2013
Arus laut adalah gerakan massa air laut yang berpindah dari satu tempat ke tempat lain.
Arus di permukaan laut terutama disebabkan oleh tiupan angin, sedang arus di kedalaman laut disebabkan oleh perbedaan densitas massa air laut. Selain itu, arus di permukan laut dapat juga disebabkan oleh gerakan pasang surut air laut atau gelombang. Arus laut dapat terjadi di samudera luas yang bergerak melintasi samudera (ocean currents), maupun terjadi di perairan pesisir (coastal currents). Penyebab utama arus permukaan laut di samudera adalah tiupan angin yang bertiup melintasi permukaan Bumi melintasi zona-zona lintang yang berbeda. Ketika angin melintasi permukaan samudera, maka massa air laut tertekan sesuai dengan arah angin.
Pola umum arus permukaan samudera dimodifikasi oleh faktor-faktor fisik dan berbagai variabel seperti friksi, gravitasi, gerak rotasi Bumi, konfigurasi benua, topografi dasar laut, dan angin lokal. Interaksi berbagai variabel itu menghasilkan arus permukaan samudera yang rumit. Karena gerakannya yang terus menerus itu, massa air laut mempengaruhi massa udara yang ditemuinya dan merubah cuaca dan iklim di seluruh dunia.
Gelombang yang datang menuju pantai membawa massa air dan momentum, searah penjalaran gelombangnya. Hal ini menyebabkan terjadinya arus di sekitar kawasan pantai. Penjalaran gelombang menuju pantai akan melintasi daerah-daerah lepas pantai (offshore zone), daerah gelombang pecah (surf zone), dan daerah deburan ombak di pantai (swash zone). Diantara ketiga daerah tersebut, Bambang Triatmodojo (1999) menjelaskan bahwa karakteristik gelombang di daerah surf zone dan swash zone adalah yang paling penting di dalam analisis proses pantai.
Menurut Dean dan Dalrymple (2002), perputaran/sirkulasi arus di sekitar pantai dapat digolongkan dalam tiga jenis, yaitu: arus sepanjang pantai (Longshore current), arus seret (Rip current), dan aliran balik (Back flows/cross-shore flows). Sistem sirkulasi arus tersebut seringkali tidak seragam antara ketiganya bergantung kepada arah/sudut gelombang datang. Pada kawasan pantai yang diterjang gelombang menyudut (αb > 5o) terhadap garis pantai, arus dominan yang akan terjadi adalah arus sejajar pantai (longshore current).
Sedangkan apabila garis puncak gelombang datang sejajar dengan garis pantai, maka akan terjadi 2 kemungkinan arus dominan di pantai. Yang pertama, bila di daerah surf zone terdapat banyak penghalang bukit pasir (sand bars) dan celah-celah (gaps) maka arus yang terjadi adalah berupa sirkulasi sel dengan rip current yang menuju laut. Kemungkinan kedua, bila di daerah surf zone tidak terdapat penghalang yang mengganggu maka arus dominan yang terjadi adalah aliran balik (back flows).
Terjadinya rip current Namun karena pengaruh hidrodinamik laut yang sangat kompleks, maka yang biasanya terjadi adalah kombinasi dari kondisi-kondisi di atas.
Macam-macam arus :
1. Arus Permukaan Laut di Samudera (Surface Circulation) disebabkan Angin Muson
Faktor utama adalah tiupan angin yang bertiup melintasi permukaan Bumi melintasi zona-zona lintang yang berbeda. Ketika angin melintasi permukaan samudera, maka massa air laut tertekan sesuai dengan arah angin. Pola umum arus permukaan samudera dimodifikasi oleh faktor-faktor fisik dan berbagai variabel seperti friksi, gravitasi, gerak rotasi Bumi, konfigurasi benua, topografi dasar laut, dan angin lokal. Interaksi berbagai variabel itu menghasilkan arus permukaan samudera yang rumit. Arus di samudera bergerak secara konstan melintasi samudera yang luas dan membentuk aliran yang berputar searah gerak jarum jam di Belahan Bumi Utara (Northern Hemisphere), dan berlawanan arah gerak jarum jam di Belahan Bumi Selatan (Southern Hemisphere). Karena gerakannya yang terus menerus itu, massa air laut mempengaruhi massa udara yang ditemuinya dan merubah cuaca dan iklim di seluruh dunia.
2. Arus di Kedalaman Samudera (Deep-water Circulation) disebabkan Proses Konveksi
Faktor utama yang mengendalikan gerakan massa air laut di kedalaman samudera adalah densitas air laut. Perbedaan densitas diantara dua massa air laut yang berdampingan menyebabkan gerakan vertikal air laut dan menciptakan gerakan massa air laut-dalam (deep-water masses) yang bergerak melintasi samudera secara perlahan. Gerakan massa air laut dalam tersebut kadang mempengaruhi sirkulasi permukaan. Perbedaan densitas massa air laut terutama disebabkan oleh perbedaan temperatur dan salinitas air laut. Oleh karena itu, gerakan massa air laut dalam tersebut disebut juga sebagai sirkulasi termohalin (thermohaline circulation).
3. Arus Pasang Surut (Tidal Current)
Arus pasang surut terjadi terutama karena gerakan pasang surut air laut. Arus ini terlihat jelas di perairan estuari atau muara sungai. Bila air laut bergerak menuju pasang, maka terlihat gerakan arus laut yang masuk ke dalam estuari atau alur sungai; sebaliknya ketika air laut bergerak menuju surut, maka terlihat gerakan arus laut mengalir ke luar.
4. Arus Sepanjang Pantai (longshore current) dan Arus Rip (rip current)
Kedua macam arus ini terjadi di perairan pesisir dekat pantai, dan terjadi karena gelombang mendekat dan memukul ke pantai dengan arah yang muring atau tegak lurus garis pantai. Arus sepanjang pantai bergerak menyusuri pantai, sedang arus rip bergerak menjauhi pantai dengan arah tegak lurus atau miring terhadap garis pantai.
5. Arus Panas dan Arus Dingin
Keduanya merupakan arus yang disebabkan perbedaan suhu air laut dengan suhu air laut disekitarnya. Arus panas terjadi jika suhu air laut lebih panas daripada air laut sekitarnya, sedang arus dingin terjadi bila suhu air laut lebih dingin dari suhu air laut sekitarnya.
6. Break Current
Arus air yang mengalir kuat ke arah laut dari sekitar pantai, biasanya melalui garis selancar, dan dapat terjadi pada setiap pantai yang bergelombang pecah. Saat angin dan gelombang laut mendorong air menuju pantai, air sering didorong menyamping oleh gelombang yang mendekat. Air ini mengalir ke sepanjang garis pantai sampai menemukan jalan keluar kembali ke laut atau ke perairan danau yang terbuka. Arus pecah yang dihasilkan biasanya sempit dan terletak di sebuah parit antara gosong pasir, di bawah dermaga atau sepanjang dermaga jetti.
Macam-macam arus laut menurut letaknya, yaitu :
- arus bawah
- arus atas
Macam-macam arus laut menurut suhunya, yaitu :
- arus panas
- arus dingin
Macam-macam arus laut menurut cara terjadinya :
- arus laut karena pengaruh tiupan angin.
- arus laut karena perbedaan kadar garam/berat jenis
- arus laut karena perbedaan tinggi rendah permukaan air laut yang disebabkan oleh pasang surut.
- arus laut karena pengaruh daratan/benua.
A. Arus di samudra pasifik
Samudra pasifik neruipakan samudra yang terluas didunia. Samudra ini dibedakam menjadi dua kelompok. Yaitu :
1.) di sebelah utara khatulistiwa
- arus khatulistiwa utara, arus panas yang bergerak menuju barat dan sejajar dengan garis khatulistiwa yang digerakkan oleh angin pasat timur laut.
- arus kuroshiwo, arus panas yang mengalir dari Filipina menuju perairan Jepang, selanjutnya ke Amerika Utara.
- arus kalifornia, arus dingin kelanjutan dari Kuroshiwo, bergerak di pesisir barat Amerika Utara ke arah khatulistiwa.
- arus oyashiwo, arus dingin dari selat Bering menuju ke selatan Kepulauan Jepang dan bertemu Arus Kuroshiwo. Pertemuan dua arus ini membuat perairan di sekitarnya kaya akan ikan, karena di temat tersebut keberadaan plankton sangat melimpah.
2.) di sebelah selatan khatulistiwa
- arus khatulistiwa selatan, arus panas yang bergerak ke barat sejajar dengan garis khatulistiwa akibat angin pasat tenggara.
- arus humboldt atau arus peru, arus laut dingin yang mengalir di pesisir barat Amerika Selatan ke arah utara.
- arus australia timur, arus laut yang bergerak di sepanjang pesisir Australia Timur ke selatan.
- arus angin barat, merupakan arus laut di Australia timur yang mengalir menuju ke timur.
B. Arus di samudra Hindia
1.) di sebelah utara khatulistiwa
- arus laut muson barat daya, arus panas yang bergerak menyusuri Laut Arab dan Teluk Benguela, akibat angin musim barat daya.
- arus laut muson timur laut, arus laut panas bergerak ke barat melalui Teluk Benguela dan Laut Arab.
2.) di sebelah selatan khatulistiwa
- arus maskarena dan arus agulhas, arus panas yang mengalir ke selatan melewati pantai Pulau Madagaskar Timur sedangkan Arus Agulhas di sebelah barat.
- arus angin barat, arus laut dingin yang menyusuri pantai barat Benua Australia ke arah utara.
C. Arus di samudra Atlantik
1.) di sebelah utara khatulistiwa
- arus Greenland timur, arus laut dingin yang bergerak dari kutub utara menuju pulau Greenland.
- arus labrador, arus dingin yang bergerak dari kutub utara ke selatan melewati pantai timur Labrador.
- arus canari, arus dingin yang bergerak melalui pesisir Spanyol dan mengalir ke selatan (pantai barat Afrika).
2.) di sebelah selatan khatulistiwa
- arus khatulistiwa selatan, arus laut panas yang bergerak ke barat, sejajar dengan garis khatulistiwa. Arus ini didorong oleh angin pasat tenggara.
- arus brazilia, arus panas yang mengalir menyusuri pantai Amerika Selatan (Brazilia) dan terus mengalir ke selatan.
- arus benguela, arus dingin yang bergerak ke arah utara menyusuri pantai barat Afrika Selatan dan yang akhirnya kembali menjadi Arus Khatulistiwa Selatan.
- arus angin barat, merupakan kelanjutan dari Arus Brazilia yang ke arah timur dan berupa arus dingin.
Metode Perolehan Data Arus
Pengukuran Arus Secara Insitu. Agar memperoleh ketepatan pengukuran yang baik, pengukuran harus dilakukan di sepanjang kolom pengukuran. Ketersediaan alat ukur (misalnya: current meter) membatasi kemampuan melakukan pengukuran secara sekaligus di satu kolom pengukuran. Arus di perairan pantai tidak bergerak dengan kecepatan yang tetap, melainkan berfluktuasi, baik secara acak maupun sistematik. Fluktuasi kecepatan arus berkisar mulai dari perioda singkat (detik) sampai panjang (jam). Fluktuasi kecepatan arus singkat dan acak dapat disebabkan oleh turbulensi dan pengaruh angin atau gelombang. Fluktuasi kecepatan arus panjang dan sistematik dapat disebabkan oleh siklus pasang surut. Status termaju teknologi pengukuran arus saat ini adalah dengan metoda akustik menggunakan ADCP yang memanfaatkan prinsip Doppler untuk mengukur kecepatan arus. ADCP mengirimkan gelombang akustik dengan frekuensi tertentu yang diketahui ke kolom air. Beberapa saat kemudian, ADCP mendengarkan pantulannya kembali dari partikel-partikel padat yang melayang dalam air. Teknologi akustik semacam ADCP memungkinkan pengukuran arus dengan akurasi tinggi. Dengan ADCP, resolusi temporal dan spasial yang tinggi untuk pengukuran arus dapat dicapai (adcpartikel.htm).
Perolehan Data Arus Dengan Satelit Altimetri
Dikutip dari www.geodesy.gd.itb.ac.id.htm, secara umum sistem satelit altimetri mempunyai tiga objektif ilmiah jangka panjang yaitu: mengamati sirkulasi lautan global, memantau volume dari lempengan es kutub, dan mengamati perubahan muka laut rata-rata (MSL) global. Dalam konteks geodesi, objektif terakhir dari misi satelit altimetri tersebut adalah yang menjadi perhatian. Dengan kemampuannya untuk mengamati topografi dan dinamika dari permukaan laut secara kontinyu, maka satelit altimetri tidak hanya bermanfaat untuk pemantauan perubahan MSL global, tetapi juga akan bermanfaat untuk beberapa aplikasi geodetik dan oseanografi seperti yang diberikan [SRSRA, 2001; Seeber, 1993]:
- Penentuan topografi permukaan laut (SST)
- Penentuan topografi permukaan es
- Penentuan geoid di wilayah lautan
- Penentuan karakteristik arus dan eddies
- Penentuan tinggi (signifikan) dan panjang (dominan) gelombang
- Studi pasang surut di lepas pantai
- Penentuan kecepatan angin di atas permukaan laut
- Penentuan batas wilayah laut, dan es
- Studi fenomena El Nino
- Manajemen sumber daya laut
- Unifikasi datum tinggi antar pulau
Begitu banyak hal yang dapat kita pelajari dengan mengaplikasikan teknologi Satelit Altimetri, sehingga teknologi ini mulai menjadi trend baru dalam dunia science dan rekayasa geodesi kelautan, oceanografi, dan bidang-bidang ilmu terkait lainnya.
Satelit Altimetri diperlengkapi dengan pemancar pulsa radar (transmiter), penerima pulsa radar yang sensitif (receiver), serta jam berakurasi tinggi. Pada sistem ini, altimeter radar yang dibawa oleh satelit memancarkan pulsa-pulsa gelombang elektromagnetik (radar) kepermukaan laut. Pulsa-pulsa tersebut dipantulkan balik oleh permukaan laut dan diterima kembali oleh satelit.
Informasi utama yang ingin ditentukan dengan satelit altimetri adalah topografi dari muka laut. Hal ini dilakukan dengan mengukur ketinggian satelit di atas permukaan laut dengan menggunakan waktu tempuh dari pulsa radar yang dikirimkan kepermukaan laut, dan dipantulkan kembali ke satelit.
Untuk mengeliminasi efek dari gelombang serta gerakan muka laut berfrekuensi tinggi lainnya, jarak ukuran adalah jarak rata-rata dalam daerah footprint. Dari data rekaman waktu tempuh sinyal kita dapat menentukan posisi vertikal permukaan laut, topografi muka laut (SST), Undulasi Geoid, Topografi es, lokasi dan kecepatan arus laut. Dari data amplitudo gelombang pantul kita dapat memperoleh informasi mengenai kecepatan angin sepanjang permukaan groundtrack satelit, dan batas laut serta es. Sementara itu dari data bentuk dan struktur muka gelombang pantul kita dapat melihat tinggi gelombang, panjang gelombang dominan, informasi termoklin, dan kemiringan lapisan es.
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