LAPORAN PRAKTIKUM HIDROLOGI
BAB I PENDAHULUAN 1.1
Latar Belakang
Terbentuknya
air
tanah
dapat
diketahui
dengan
memperhatikan distribusi air bawah permukaan dan struktur zona
geologi
menghasilkanair.
yaitu Hampir
kemampuan seluruh
air
menangkap tanah
dan
diperkiraka
merupakan bagian dari siklus hidrologi, termasukair permukaan dan air atmosfir (meteor). Keberadaan dan umur air tanah telah sering dibicarakan, dan radioisotop dapat digunakan untuk menentukan umur air tanah.Hidrogen-3 (tritium) dan karbon-14 adalah dua isotop yang terbukti sangat bermanfaat untuk menentukan umur air tanah. Penelitian adalah kegiatan yang dilakukan oleh seseorang yang melalukan kegiatan lapangan yang menjadi bahan acuan yang mendominasi untuk mengtehui apa yang belum diketahui. Karena semua fenomena hidrologi berubah menurut waktu, maka disebut disebut penelitian yang dibarengi dengan hukm kepastian, proses tersebut tidak tergantung pada peluang. Aliran air tanah merupakan
contoh
proses
deterministik.
Karena
laju
liran
sebanding dengan gradien hidrolik. Proses determinasi juga merupakan yang tidak berubah karena waktu. Tetapi jika perubahan variabel merupakan faktor peluang, prosesnya dinamakan statistik atau probabilistik. Pada umumnya proses statistik sebagai proses yang tidak tergantung waktu. Lengkung durasi aliran air bawah tanah merupakan contoh proses probalistik dan kebanyakan proses hidrologi termasuk termasuk proses statistik. Proses hidrologi terdiri dari kompnenkomponen deterministik dan statistik. besasrnya kadar masing-
1
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LAPORAN PRAKTIKUM HIDROLOGI
masing komponen tersebut dapat diselesaikan secara dinamistik dan
ststistik.
matematis
Karena
sangat
proses-proses
sulit,
maka
non
stasioner
proses-proses
secara hidrologi
diselesaikan secara stasioner. stasioner. Ilmu hidrologi dapat dibagi menjadi hidrologi paramatik dan hidrologi stakastik. Hidrologi parmatik didefenisikan sebagai pengembangan
dan
analisis
hubungan
antara
parameter-
parameter fisik yang dimasukan kedalam kejadian sintesa kejadian-kejadian
hidrologi
studi
dan
penelitian
hidrologi
parametrik dapat melibatkan penggunaan model-model fisik analog dan digital atau analisis fisik tradisional. Salah satu penerapan yang penting adalah penataan kembali urutan waktu kejadian-kejadian
hidrologi
yang
historik
dan
usaha
menghasilkan urutan nonhistorik yang representatik. 1.2 Maksud Dan Tujuan Maksud dan tujuan penelitian ini dilakukan yang tiada lain hanyalah untuk: a. untuk mangetahui pola aliran air bawah tanah mengenai tata cara aliran air bawah tanah. b. Mengikuti lapangan
dan
berkompetensi
hidrologi
yang
aktif
dilakukan
dalam untuk
praktikum
penambahan
wawasan yang ,dikaji dalam Ilmu geografi . c. Membarikan rasa kekompakan yang bersifat positif dan sikap kerjasama antar mahasiawa program studi geografi. d. Untuk mengetahui arah pergerakan air bawah tanah 1.3
Nama acara Nama acara yang dilakukan pada penelitian ini yaitu :
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LAPORAN PRAKTIKUM HIDROLOGI
1.4 Manfaat Praktikum atau penelitian yang dilakukan pada periode ini “pola aliran air sungai" pada penelitian ini diharapkan dapat
memberikan manfaat untuk melakukan penelitian berikutnya. Adapun garis-garis besar mengnai manfaat yang dapat dirasakan dalam penelitian ini adalah: 1. Memberikan tata cara pengolahan air bawah tanah. 2. Bagimana cara dalam pembuatan peta kontur mengenai pola aliran air bawah tanah. 1.5 Alat dan Bahan Alat dan bahan yang kami butuhkan pada penelitian ini adalah: 1. Roll meter 2. GPS 3. Alat pengukur kedalaman sumur 4. Sumur-sumur warga 5. Kalkulator 6. Peta dasar 7. Alat tulis menulis
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LAPORAN PRAKTIKUM HIDROLOGI
BAB II TEORI SINGKAT
2.1 Dasar Teori Menurut Herlambang (1996) air tanah adalah air yang bergerak di dalam tanah yang terdapat didalam ruang antar butir-butir tanah yang meresap ke dalam tanah dan bergabung membentuk lapisan tanah yang disebut akifer. Lapisan yang mudah dilalui oleh air tanah disebut lapisan permeable, seperti lapisan yang terdapat pada pasir atau kerikil, sedangkan lapisan yang sulit dilalui air tanah disebut lapisan impermeable, seperti lapisan lempung atau geluh. Lapisan yang dapat menangkap dan meloloskan air disebut akuifer. Menurut Krussman dan Ridder (1970) dalam Utaya (1990) bahwa macam-macam akifer sebagai berikut: a. Akifer Bebas (Unconfined Aquifer) yaitu lapisan lolos air yang hanya sebagian terisi oleh air dan berada di atas lapisan kedap air. Permukaan tanah pada aquifer ini disebut dengan water table (preatiklevel), yaitu permukaan air yang mempunyai tekanan hidrostatik sama dengan
atmosfer.
b. Akifer Tertekan (Confined Aquifer) yaitu aquifer yang seluruh jumlahnya air yang dibatasi oleh lapisan kedap air, baik yang di atas maupun di bawah, serta mempunyai tekanan jenuh lebih besar dari pada tekanan atmosfer. c. Akifer Semi tertekan (Semi Confined Aquifer)
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LAPORAN PRAKTIKUM HIDROLOGI
yaitu aquifer yang seluruhnya jenuh air, dimana bagian atasnya dibatasi oleh lapisan semi lolos air dibagian bawahnya merupakan lapisan kedap air. d. Akifer Semi Bebas (Semi Unconfined Aquifer) yaitu aquifer yang bagian bawahnya yang merupakan lapisan
kedap
air,
sedangkan
bagian
atasnya
merupakan
material berbutir halus, sehingga pada lapisan penutupnya masih memungkinkan adanya gerakan air. Dengan demikian aquifer ini merupakan peralihan antara aquifer bebas dengan aquifer semi tertekan. Tolman (1937) dalam Wiwoho (1999) mengemukakan bahwa air tanah dangkal pada akifer dengan material yang belum termampatkan di daerah beriklim kering menunjukan konsentrasi unsur-unsur kimia yang tinggi terutama musim kemarau. Hal ini disebabkan oleh adanya gerakan kapiler air tanah dan tingkat evaporasi yang cukup besar. Besar kecilnya material terlarut tergantung pada lamanya air kontak dengan batuan. Semakin lama air kontak dengan batuan semakin tinggi unsur-unsur yang terlarut di dalamnya. Disamping itu umur batuan juga mempengaruhi tingkat kegaraman air, sebab semakin tua umur batuan, maka semakin tinggi pula kadar garam-garam yang terlarut di dalamnya. Todd (1980) dalam Hartono (1999) menyatakan tidak semua formasi litologi dan kondisi geomorfologi merupakan akifer yang baik. Berdasarkan pengamatan lapangan, akifer dijumpai pada bentuk lahan sebagai berikut: a. Lintasan air (water course), materialnya terdiri dari aluvium
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LAPORAN PRAKTIKUM HIDROLOGI
dataran banjir serta tanggul alam. Bahan aluvium itu biasanya berupa pasir dan karikil. b. Lembah yang terkubur (burried valley) atau lembah yang ditinggalkan (abandoned valley), tersusun oleh materi lepaslepas yang berupa pasir halus sampai kasar. c. Dataran (plain), ialah bentuk lahan berstruktur datar dan tersusun atas bahan aluvium yang berasal dari berbagai bahan induk sehingga merupakan akifer yang baik. d. Lembah antar pegunungan (intermontane valley), yaitu lembah yang berada diantara dua pegunungan, materialnya berasal dari hasil erosi dan gerak massa batuan dari pegunungan di
sekitarnya.
e. Batu gamping (limestone), air tanah terperangkap dalam retakan-retakan atau diaklas-diaklas. Porositas batu gamping ini bersifat sekunder. 1. Gerakan Air Tanah Disamping air tanah bergerak dari atas ke bawah, air tanah juga bergerak dari bawah ke atas (gaya kapiler). Air bergerak horisontal pada dasarnya mengikuti hukum hidrolika, air
bergerak
horisontal
karena
adanya
perbedaan
gradien
hidrolik. Gerakan air tanah mengikuti hukum Darcy yang berbunyi “volume air tanah yang melalui batuan berbanding
lurus dengan tekanan dan berbanding terbalik dengan tebal lapisan (Utaya, 1990). 2. Kondisi Air Tanah Dataran Alluvial Dataran alluvial merupakan dataran yang terbentuk akibat
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LAPORAN PRAKTIKUM HIDROLOGI
topografi, suhu, yang semuanya akan mempercepat proses pelapukan dan erosi. Hasil erosi diendapkan oleh air ketempat yang lebih rendah atau mengikuti aliran sungai. Dataran alluvial menempati daerah pantai, daerah antar gunung, dan dataran lembah sungai. Air tanah daerah dataran pantai selalu terdapat dalam sedimen kuarter dan resen yang batuannya terdiri dari pasir, kerikil, dan berinteraksi berinteraksi dengan lapisan l apisan lempung. Pengertian susunan litologi dari butir kasar ke halus membentuk suatu kondisi air tanah tertekan, cekungan cekungan air tanah antar gunung mempunyai potensi yang cukup besar. Beberapa bentuk lahan asal fluvial adalah sebagai berikut : (1) Kipas Alluvial (Alluvial fan); (2) Crevasse-Splays; (3) Tanggul alam (Natural lever); (4) Poin bar; (5) Dataran banjir; (6) Cekungan fluvial (Flood plain); (7) Teras Alluvial; (8) Delta Volume air tanah dalam dataran alluvial di tentukan oleh tebal dan penyebaran permeabilitas dari akifer yang terbentuk dalam aluvium dan dilluvium yang mengendap
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LAPORAN PRAKTIKUM HIDROLOGI
dapat dengan sumur dangkal. Dataran alluvial unsur-unsur yang dominan adalah unsur NO2, NO3, Ca, Mg, Si, dan Fe. Kelebihan Nitrit karena pengaruh zat buangan (urine), pembusukan pembusukan organik dari hasil reduksi nitrat yang ada disekitar air tanah (Karmono dan Joko Cahyo, 1978:11). Hal ini selain dipengaruhi oleh faktor alam juga sebagai aktivitas manusia misalnya adanya lahan pertanian yang mengkonsumsi pupuk organik yang men gandung nitrat. 3. Asal-Usul dan Sifat-Sifat Air Tanah Adalah hal yang mutlak bagi para birokrat pengelola sumber daya air (tanah), untuk memahami asal-usul (origin) dan sifat-sifat
(nature)
air
tanah,
agar
pengertian
tentang
sumberdaya
pengertian
tersebut
akan
tidak
yang
menjadikan
terjadi
dikelola. tujuan
kesalahKesalah-
mewujudkan
kemanfaatan air tanah terutama bagi kaum miskin pengelolaan tidak mencapai sasarannya, bahkan justru akan menimbulkan dampak yang merugikan bagi keterdapatan air tanah itu sendiri serta kaum miskin tersebut. Hal-hal pokok yang perlu dipahami tentang asal-usul dan sifat-sifat air tanah adalah : (1) Pembentukan Air Tanah
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LAPORAN PRAKTIKUM HIDROLOGI
peristiwa yang selalu berulang dari urutan tahap yang dilalui air dari atmosfer ke bumi dan kembali ke atmosfer; penguapan dari darat atau laut atau air pedalaman, pengembunan membentuk awan, pencurahan, pelonggokan dalam tanih atau badan air dan penguapan kembali (Kamus Hidrologi, 1987). Dari daur hidrologi tersebut dapat dipahami bahwa air tanah berinteraksi dengan air permukaan serta komponen-komponen lain yang terlibat dalam daur hidrologi termasuk bentuk topografi, jenis batuan penutup, penggunaan lahan, tetumbuhan penutup, serta manusia yang berada di permiukaan. Air tanah dan air permukaan saling berkaitan
dan
berinteraksi.
Setiap
aksi
(pemompaan,
pencemaran dll) terhadap air tanah akan memberikan reaksi terhadap air permukaan, demikian sebaliknya. (2) Wadah Air Tanah Suatu formasi geologi yang mempunyai kemampuan untuk menyimpan dan melalukan air tanah dalam jumlah berarti ke sumur-sumur atau mata air – mata air disebut akuifer. Lapisan pasir atau kerikil adalah salah satu formasi geologi yang dapat bertindak sebagai akuifer. Wadah air tanah yang disebut akuifer tersebut dialasi oleh lapisan lapisan batuan dengan daya
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LAPORAN PRAKTIKUM HIDROLOGI
tekanan udara luar. Semua akuifer mempunyai dua sifat yang mendasar: (i) kapasitas menyimpan air tanah dan (ii) kapasitas mengalirkan air tanah. Namun demikaian sebagai hasil dari keragaman geologinya, akuifer sangat beragam dalam sifat-sifat hidroliknya (kelulusan dan simpanan) dan volume tandoannya (ketebalan dan sebaran geografinya). Berdasarkan sifat-sifat tersebut akuifer dapat mengandung air tanah dalam jumlah yang sangat besar dengan sebaran yang luas hingga ribuan km2 atau sebaliknya. Ditinjau dari kedudukannya terhadap permukaan, air tanah dapat disebut (i) air tanah dangkal (phreatic), umumnya berasosiasi dengan akuifer tak tertekan, yakni yang tersimpan dalam akuifer dekat permukaan hingga kedalaman – tergantung kesepakatan – 15 sampai 40 m. (ii) air tanah dalam, umumnya berasosiasi dengan akuifer tertekan, yakni tersimpan dalam akuifer pada kedalaman lebih dari 40 m (apabila kesepakatan air tanah dangkal hingga kedalaman 40 m). (3) Pengaliran dan Imbuhan Air Tanah Air tanah dapat terbentuk atau mengalir (terutama secara horisontal), dari titik /daerah imbuh (recharge), seketika itu juga pada saat hujan turun, hingga membutuhkan waktu harian,
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LAPORAN PRAKTIKUM HIDROLOGI
(4) Mutu Air Tanah Sifat fisika dan komposisi kimia air tanah yang menentukan mutu air tanah secara alami sangat dipengaruhi oleh jenis litologi penyusun akuifer, jenis tanah/batuan yang dilalui air tanah, serta jenis air asal air tanah. Mutu tersebut akan berubah manakala terjadi intervensi manusia terhadap air tanah, seperti pengambilan air tanah yang berlebihan, pembuangan libah, dll Air tanah dangkal rawan (vulnerable) terhadap pencemaran dari zat-zat pencemar dari permukaan. Namun karena tanah/batuan bersifat
melemahkan
zat-zat
pencemar,
maka
tingkat
pencemaran terhadap air tanah dangkal sangat tergantung dari kedudukan akuifer, besaran dan jenis zat pencemar, serta jenis tanah/batuan di zona takjenuh, serta batuan penyusun akuifer itu sendiri. Pola aliran air tanah merupakan salah satu kajian ilmiah yang menjadi bahan acuan dalam bidang ilmu geografi yang menjadikan segala bentuk pengolahan dan tata cara dalam meneliti pola aliran air sungai. sungai. Pola Pola
aliran sungai sungai merupakan merupakan
daerah di sekitar air tanah tempat air hujan terapung dan tempat dimana air hujan dialirkan kedalam tanah. Pada pola aliran air bawah tanah ini dilaksanan melalui
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LAPORAN PRAKTIKUM HIDROLOGI
Hidrologi berasal dari bahasa yunani : “ ilmu air “ adalah
cabang
ilmu
tekhnik
sipil
yang
mempelajari
pergerakan,
distribusi dan kwalitas air diseluruh bumi. Termasuk siklus hidrologi dan sumber daya air. Orang yang ahli dalam bidang hidrologi disebut disebut hidrolog, hidrolog, bekerja dalam dalam bidang ilmu bumi dan dan ilmu lingkungan serta tekhnik sipil dan tekhnik lingkungan. Hidrologi juga meliputi hidrometeorologi, hidrometeorologi, hidrologi air permukaan hidrogeologi manajemen, limbah, dan kwalitas air, dimana air memiliki peranan penting. Oceanografi dan meteorologi tidak termasuk karena air hanya satu dari aspek penting lainnya. Hidrologi juga memiliki kegunaan
lebih
lanjut
bagi
tekhnik
lingkungan,
kebijakan
lingkungan, serta perencanaan. Hidrologi juga mempelajari hujan terutama meliputi periode ulang curah hujan karena berkaitan dengan perhitungan banjir serta rencana untuk setiap bangunan tekhnik sipil luas antara lain: bendung, bendungan
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LAPORAN PRAKTIKUM HIDROLOGI
d. Apklikasi teori-teori hidrologi unruk memecahkan masalah praktis. Pergerakan air dipermukaan bumi dinamakan siklus air. Suklus air atau siklus hidrologi adalah sirkulasi air yang tidak pernah berhanti dari atmosfer kebumi dan kembali keatmosfer melalui
kondensasi,
presipitasi,
evaporasi
dan
transpirasi.
Pemanasan air samudra oleh sinar matahari merupakan kunci proses silus hidrologi tersebut dapat berjalan secara kontinue. Air berevaporasi, kemudian jatuh sebagai presipitasi dalam bentuk hujan, salju, hujan es, dan hujan gerimis atau kabut. Hidrologi
bukanlah
ilmu
yang
berdiri
sendiri,
tetapi
ada
hubungannya dengan ilmu lain, seperti meteorolgi, klimatologi, geologi, agronomi kehutanan, dan ilmu tanah dan hidrolika. Menurut the Internnational assocition of scientific hidrologi, hidrologi dapat dibagi menjadi: a. Patamologi khususnya mempelajari aliran permukaan
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LAPORAN PRAKTIKUM HIDROLOGI
kemudian jatuh kkepermukaan tanah lagi sebagai hijan auatu bentuk presipitasi lain, dan akhinya mengalir kelaut kembali. 2.1.2 Pengukuran muka air tanah Pengukuran muka air tanah dilakukan dengan menggunakan roll meter yang dilakukan secara manual dengan mengukur langsung kedalaman muka air tanah. Adapun yang dimaksud dengan debit adalah satuan besaran air yang keluar dari daerah aliran sungai
(Das) yang sumber sumber airnya berasal dari bawah
tanah. Satuan debit yang duganakan dalam sistem satuan SI adalah meter kubik perdetik (m 3 /detik). Mnurut asdak (2002), debit aliran air bawah tanah adalah laju aliran air yang melewati pola aliran air bawah tanah. Dalam sistem SI besarnya debit dinyatakan dalam satu meter kubik. Debit aliran merupakan ukuran banyaknya volume air yang dapat lewat dalam suatu tempat atau yang dapat ditampung dalam suatu tempat tiap satu satuan waktu.
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LAPORAN PRAKTIKUM HIDROLOGI
didalam fluida. Hal ini sulit karena kita harus menyatakan koorfinat X,Y,Z dari patikel fluida dalam menyatakan ini sebagai fungsi waktu. Cara yang digunakan adalah dengan penerapan kinematika partikel gerak atau aliran fluida. Cara untuk mengukur pola aliran air tanah adalah dengan : a. Mengukur kedalaman air sumur b. Mencatat tinggi permukaan air yang ada dalam sumur warga c. Mencatat letak astronomis daerah tersebut d. Menggunakan
pengukur
kedalaman
seperti
meteran,
tongkat berskala dll. 2.1.3 Asal Usul Air Tanah Tanah
merupakan
hal
yang
paling
mutlak
dalam
kemhidupan sehari-hari kerena tanah merupakan tempat dimana kita mencari hidup daln berrpijak maka tanah merupakan hal\ yang paling mendominasi dalam kehidupan kita.
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LAPORAN PRAKTIKUM HIDROLOGI
4. Melnjutkan dengan mengukur muka air tanah dengan menggunakan roll meter 5. Selanjutnya mmengukur diameter sumur dengan menggukan roll meter 6. Maka setelah itu melakukan pencatatan data dari hasil pengamatan seperti mencatat titik koordinat, elevasi, ketinggian dan kedalamamn. 2.4 Hasil Pengamatan Berikut adalah data yang kami dapatkan pada praktikum yang kami lakukan di kec.kota timur kota gorontalo 2.5
Hasil dan Pembahasan
TABEL PENGAMATAN
Nama Observer
: Nila Kusuma
Kelompok
: III ( tiga)
Lokasi Pengamatan
: Kec. Kota Timur Kota Gorontalo Gorontalo
Hari/Tanggal
: Senin, 18 Juli 2010
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LAPORAN PRAKTIKUM HIDROLOGI
E 123003’4,2” 6
HU6 N00032’47,34”
14
0,38
13,62
13
0,34
12,66
12
0,74
11,26
6
0,28
5,72
14
0,27
13,73
E123003’0,06” 7
HU7 N 00032’41,1” E123003’0,72”
8
HS1 N 00032’14,04” E123003’59,94”
9
HS2 N 00032’17,16” E 123003’57,3”
10
HS3 N 00032’12,84”
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LAPORAN PRAKTIKUM HIDROLOGI
E123004’35,64” 20
TM5 N 00032’18,9”
10
2,08
7,92
11
1,97
9,03
7
0,58
6,42
5
0,60
4,40
7
1,16
5,84
E123004’38,94” 21
TM6 N 00032’20,7” E123004’38,94”
22
TM7 N 00032’29,34” E123004’44,64”
23
TM8 N 00032’19,38” E 123004’59,7”
24
TM9 N 00032’10,5”
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LAPORAN PRAKTIKUM HIDROLOGI
34
LYS4 N 00029’27,78”
9
1,18
7,82
9
1,82
7,18
8
0,85
7,15
6
1,02
4,98
7
1,45
5,55
E 123004’45,6” 35
LYS5 N 00029’32,94” E123004’42,36”
36
LYU1 N 00030’0,84” E 123004’3,78”
37
LYU2 N 00030’2,16” E 123004’2,82”
38
LYU3 N 00030’3,48” E 123004’2,4”
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LAPORAN PRAKTIKUM HIDROLOGI
48
BG4 N 00031’45,36”
5
1,85
3,15
6
1,03
4,97
5
1,44
3,56
7
1,51
5,49
4
1,82
2,18
E123003’51,48” 49
BG5 N 00031’46,38” E123003’50,88”
50
IP1 N 00031’52,92” E 123004’2,28”
51
IP2 N 00031’53,94” E 123004’3,42”
52
IP3 N 00031’51,9” E 123004’2,88”
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LAPORAN PRAKTIKUM HIDROLOGI
2.6 PETA KONTUR Peta kontur yang tergambar dibawah ini merupakan peta kontur pola aliran muka air tanah kecamatan kecamatan kota timur kota gorontalo tempat tersebut merupakan tempat kami melakukan penelitian 1
28 27 0. 9
26 25 24
0. 8
23
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LAPORAN PRAKTIKUM HIDROLOGI
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LAPORAN PRAKTIKUM HIDROLOGI
Titik-Titik Koordinat Untuk Memplot Peta Kedalaman Kedalaman Muka Air Tanah No
X
Y
Z
1.
0.23
0.55
28.4
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LAPORAN PRAKTIKUM HIDROLOGI
25
0.78
0.59
16.82
26.
0.77
0.58
18.76
27.
0.74
0.62
17.52
28.
0.76
0.66
13.68
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LAPORAN PRAKTIKUM HIDROLOGI
52.
0.87
0.05
2.18
53.
0.82
0.07
1.81
54.
0.87
0.07
3.9
55.
0.54
0.16
4.72
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LAPORAN PRAKTIKUM HIDROLOGI
BAB III PENUTUP 3.1
Kesimpulan Pola aliran air tanah merupakan salah satu kajian ilmiah
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LAPORAN PRAKTIKUM HIDROLOGI
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LAPORAN PRAKTIKUM HIDROLOGI