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|Maps; Google Map Link
|(*only for information);
|Mt. Tangkuban Perahu;
|The existence of Mount Tangkuban Perahu and topography form of Bandung in the form of hollow with hills and mountains on each side strengthen the theory of the existence of a large lake which is now the area of Bandung.
It is believed by geologists that the highlands of Bandung with an altitude of approximately 709 m above sea level are the remnants of a large lake formed from the damming of the Ci Tarum river by an ancient volcanic eruption known as Mount Sunda and Mount Tangkuban Parahu, Ancient Sunda Mountain is still active.
This phenomenon can be seen on Mount Krakatau in the Sunda Strait and Ngorongoro region in Tanzania, Africa.
So the legend of Sangkuriang which is a community story of the area is believed to be a documentation of the community of the Sunda Purba area against events at that time.
|Mt. Tangkuban Perahu Nature Reserve; Mt. Tangkuban Perahu Nature Tourist Park;
|City / Regency
- Kabupaten Bandung Barat
- Kabupaten Purwakarta
- Kabupaten Subang
||1.1 Kecamatan Lembang; 1.2 Kecamatan Parongpong;
2.1 Kecamatan Bojong; 2.2 Kecamatan Wanayasa
3.1 Kecamatan Serangpanjang; 3.2 Kecamatan Sagalaherang
||1.1.1 Desa Sukajaya; 1.1.2 Desa Jayagiri; 1.1.3 Desa Cikahuripan;
1.2.1 Desa Karyawangi
2.1.1 Desa Pasanggrahan; 2.1.2 Desa Cihanjawar
2.2.1 Desa Babakan
3.1.1 Desa Cipancar
3.2.1 Desa Cicadas
|a vulcano / active
|History of eruption;
|The Tangkubanparahu eruption is characterized by a small, intensity explosive eruption and is sometimes interspersed by phreatic eruptions with an inter-eruption range of between 2 and 50 years. The history of eruptions can be described as follows:
1829: Eruption of ash and rock from the Queen’s Crater and Domas.
1846: Eruption occurred, increased activity
1896: Formed a new fumarole to the north of the Rhino crater.
1900: Steam eruption from Kawah Ratu
1910: The smoke column rises as high as 2 km above the crater wall, the eruption comes from Kawah Ratu
1926: Phreatic eruption in the Queen’s Crater forms the Ecoma hole
1935: The new fumarole field called Rhinos occurs, 150 m south-southwest of the Ratu Crater
1952: The ash eruption is preceded by a hydrothermal eruption (phreatic)
1957: Phreatic eruption in Kawah Ratu, new crater hole formed
1961,1965,1967: Phreatic eruptions
1969, 1971: Phreatic eruption is preceded by a weak eruption producing ash
1983: Phreatic eruption
1992: Ash cloud rises as high as 159 m above Kawah Ratu
1994: Strong activity increases with shallow seismic earthquakes with small phreatic eruptions
2004: Appreciation of seismicity
|Elevation (meters above sea level);
|2.084 m (6.837 ft)
|Type of eruption;
|According to van Bemmelen (1934, in Kusumadinata 1979) that Mount Tangkubanparahu grows within the eastern Sunda Caldera. Based on the pattern, Mount Tangkubanparahu eruption can be divided into three phases:
An explosive phase that produces pyroclastic and leads to lava.
The effusive phase that produces many lava flows is composed of andesite basaltis.
The formation / growth phase of Tangkubanparahu is now generally explosively small and sometimes interspersed with phreatic eruptions.
The eruption of Mount Tangkubanparahu can be classified as a small eruption. Lava linings are estimated to occur. Based on the experience since the 19th century, this volcano never showed a big magmatic eruption except the eruption of ash without being followed by lava leleran, hot clouds or incandescent stone. Phreatic eruptions are predominantly dominant and are usually followed by increases in the temperature of the solfatara and fumaroles in some of the active craters of the Ratu Crater, New Crater, and Domas Crater. The volcanic material is generally dredged ash which is limited around the peak area up to several kilometers. Mudflow is only limited in the area around the crater. At the time of increased activity, fumarola / solfatara white smoke is sometimes followed by increases in volcanic gases such as CO and CO2 toxic gases. When the accumulation of toxic gases around the active crater is higher, the region can be classified into a limited primary hazard area. Secondary hazards such as lava floods have not occurred in history. Local landslides occur in craters and steep uphill slopes.
|Topology & Geology;
|Mount Tangkubanparahu and other volcanoes located around Bandung are located in Bandung Zone (van Bemmelen, 1934 in Hadisantono et al., 1983). The Bandung Zone is a depression basin that extends between the mountains. The basin has a width of 25 – 50 km, slightly convex to the north, located between the Bogor Zone and the Southern Mountain Zone. Bemmelen (1949) states that in general this zone resides in the peak structure of geographic Java Island, which is magnified after or at the same time as the appointment that occurs at the end of Tertiary. Its geanticline axis is the place where the Quaternary Volcano is located. This volcanic belt or magmatic path extends from Pelabuhan Ratu Bay on the western part of P. Java, then passes between the Cimandiri valley with the city of Sukabumi (600 m), Cianjur plain (495 m) and Garut (711 m) to Citanduy valley with Tasikmalaya city (351 m) on the east, and ends at Segara Anakan on the southern coast of Java Island. The center of this zone is occupied by the highlands of Bandung and Garut.
Lembang fault is the largest fault in this area, which runs from west to east. This fault is located or through Lembang, 10 km north of Bandung. This is an active fault with a very clear fault escarpment facing north. This fault of a total length of approximately 22 km can be observed as a straight line from G. Palasari in east to west near Cisarua. Initial investigations have linked that the dominant Lembang fault was a normal fault occurring after the massive G. Sunda eruption that took place in the Quaternary period.
|Meteorology Climatology and Geophysics Council check…