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Identification of Cimandiri Fault Activity at Area, West , (Based on Morphometry Analysis)

Abs. No. 29 Supartoyo, Imam A. Sadisun, Emmy Suparka, Chalid Idham Abdullah Faculty of Earth Science and Technology, ITB

Sri Hidayati Center for Volcanology and Geological Hazard Mitigation, Geological Agency

ABSTRACT：Sukabumi is one of the areas in Indonesia which is prone to the earthquake. The earthquake sources are concentrated along the subduction zone which correspond to convergent plate boundaries and the active fault zones. Sukabumi had experienced several destructive earthquakes of shallow depths. In this area a famous fault zone lies along Cimandiri valley called Cimandiri fault. It lengthens from to the south of central city Sukabumi and continues to the Cianjur area. Combination of Landsat and Shuttle Radar Topography Mission (SRTM) shows 2 lineaments at the Cimandiri valley which are W-E in the western and NE-SW in the eastern. Further analysis based on landsat, SRTM and field observation, the Cimandiri Fault can be divided into 4 segments, namely segment 1, 2, 3 and 4. Morphometry analysis uses to identify activity of Cimandiri fault compose of six parameters namely drainage basin asymmetry (AF), hypsometric, stream length gradient index (SL), mountain front sinuosity (Smf), valley floor width - valley height ratio(Vf) and drainage basin shape indices (Bs). The result found that AF is far from value of 50 indicates the presence of tectonic tilting, the hypsometric curve shows that most of the Cimandiri Fault belongs to young topography. Meanwhile the SL is more than 300 indicating of active tectonic, Smf value is less than 1,5 indicating straight of mountain front sinuosity as a Cimandiri Fault Zone, Vf less than 2 shows most of V shape valley and Bs mean is more than 2 shows elongated drainage basin along Cimandiri Fault Zone. All the morphometry para- meters analysis indicates that the Cimandiri Fault is an active fault and in the segment 3 and 4 that located in eastern parts of Cimandiri fault are more active than segment 1 and 2. The destructive earthquake in 1982 with magnitude 5.5 RS was probably related to the segment 3 and 4 of Cimandiri Fault.

1. Introduction active fault based on epicenter distribution along Sukabumi area is located at the western part of Cimandiri Fault Zone (Soehaimi et al., 2004 and Province, boundary by Cianjur in 2007; Kertapati 2006) and its movement by GPS the east, regency in the north, prov- (Abidin 2008). In this study the activities of CF ince in the west and Indian Oceanic in the south. The would be analyzed using geomorphic and morpho- area is one of the areas in Indonesia which vulnera- metric analyses. ble to the earthquake. The earthquake sources are concentrated along the subduction zone, which cor- 2. Tectonic and Geological Setting respond to convergent plate boundaries and the ac- The Indonesia archipelago is resulted from inte- tive fault zones. This area had experienced several raction amongst four active plates: Hindia-, destructive earthquakes of shallow depths. These Eurasia, Pasific and Philippine. The Hindia- earthquakes had caused victim and damaged build- Australia plate moves to the northeast with velocity ing in this area. The destructive earthquake events 7 cm/ year, Eurasia plate to the south (0.4 cm/ year), generally when the earthquake has an epicenter lo- Pacific plate to the west (11 cm/ year) and Philippine cated in land and shallow depth, such as occurred in sea plate to the northwest with velocity 8 cm/ year 1962, 1973, 1975, 1977, 1982 and 2000 (Supartoyo (Minster and Jordan, 1978 in Yeats et. al., 1997). and Surono, 2008). The western part of Indonesia is mostly affected by In Sukabumi area, there is a fault zone lies along interaction between Hindia-Australia and Eurasia Cimandiri valley called Cimandiri Fault (CF). Its plate. It causes the formation of Java-Sumatera length stretches from Palabuhanratu bay to the south trench, Java–Sumatera fore arc basin, the Java– of central city Sukabumi and continues to the Cian- Sumatera outer arc partly submerged south of Java, jur area. Previous studies suggested that CF was an Java and Sumatera magmatic arc, foreland basin of

Proceeding of 1st International Seminar of Environmental Geoscience in Asia (ISEGA I), Oktober 2013, page 76 – 83. the Sunda continental shelf, pull apart basin in Su- CF as a reverse fault and inactive fault. The field ob- matera and Java–Sumatera back arc basin. Apart servation along Cimandiri valley showed manifesta- from that, it also produced of earthquake source in tion of this fault such as fault scarp, slicken side, the sea along subduction zone and inland from ac- fault breccias, drag fault, broken zones, lineament of tive fault. This condition makes Indonesia prone to spring water, valley and triangular facets. geological hazard especially earthquake and tsuna- mi. 3. Methods Based on the physiographic map of West Java In this study we analyze the activities of CF using (Bemmelen,1949) and geological setting (Martodjo- morphometry parameters. Morphometry is defined jo, 2003), West Java can be divided into three trend- as quantitative measurement of landscape and land- ing belts from north to the south which are the low form shape (Keller and Pinter, 1996). Quantitative plain of reflecting the shelf basinal area; the measurement allows geomorphologist to objectively Bogor zone a shelf edge with deep basinalturbidite compare different landform and to calculate less sediments were accumulated, folded and thrusted; straightforward parameters (geomorphic indicates). the southern mountains of West Java. The Cimandiri This information is very useful for identifying a par- Fault Zone (CFZ) is located south of Bogor zone and ticular characteristic an area to identify of tectonic mostly covered by young volcanic deposits. Based activity level. This method can be used for rapid of on morphogenetic unit the Sukabumi area is sepa- tectonic evaluation for large areas. Also this method rated by volcanic folded hills and mountain and vol- is very easy to do and the data can be obtained from canic arc of Sunda/ Banda system (Verstappen, topography maps and aerial photographs (Keller and 2000). This separated lies on CFZ. Pinter, 1996). Field observation divided morphology of Suka- Morphometry analyses have been applied to ana- bumi area into three zones, which are flat, moderate lyze the activities of several faults, such as to ana- and steeply hills. The flat occupies the coastal area, lyze fault activities in Vulcanic Trans-Mexican along Cimandiri valley and northeast of Sukabumi. based on Digital Elevation Model (DEM) resolu- Elevation of the coastal area is less than 10 m com- tion 50 m and topography map scale 1 : 50.000 prising Palabuhanratu, Simpenan, Ciemas, Cisolok, (Szynkaruk et al., 2004), to analyze activities of Ciracap, Surade, Cibitung and Tegalbuleud. Several Kompotadesdan NeaAchialos fault in Yunani based coastal areas are hilly with elevation about 50 m and on topography map scale 1 : 50.000 (Zovoili et al., steeply with exposed lava and sandstone in Simpe- 2004), to analyze active deformation on Pannonian- nan, Ciemas and Cisolok. Hungaria basin based on topography map scale Steeply to moderate hills are dominant around 1 : 200.000 and 1 : 50.000 (Pinter, 2005), to analyze Sukabumi area where Cimandiri River runs perpen- activities of North Anatolian Fault topography map dicular through the area to Palabuhanratu Bay. The scale 1 : 25.000 (Gurbuz and Gurer, 2008). Cimandiri valley lies in west-east direction, starting In this analysis topographic map with scale from Palabuhanratu Bay to Warungkiara and bend to 1:25.000 is used to calculate the morphometry pa- southwest- northeast from Cikembar to the southern rameters. This map was published by Badan Koor- of Sukabumi. Mostly of Sukabumi area is covered dinasi Survei dan Pemetaan Nasional (Bakosurtanal) by quaternary deposit such as young volcanic depo- and composed of 11 sheets, namely Balewer, Cida- sits and alluvial. These quaternary deposits are vul- dap, Cigenca, Jampang Tengah, Nyalindung, Tako- nerable to earthquake, due to loose and unconsoli- kak, Palabuhanratu, Cigombong, Cibadak, Sukabu- dated. mi and Gegerbitung. The main manifestation along Cimandiri valley is CFZ. This zone stretches from Palabuhanratu Bay to 4. Geomorphic and Morphometric Analyses area and occupies between Bandung zone The topography of the CF in the study area is a and the southern mountains. Using landsat image, valley lengthening from Palabuhanratu bay to the Suwijanto (1978) identified CF from the lineament southern of Sukabumi city. In the western part the and several earthquake events along the Cimandiri trend of valley is west – east and in the middle turn valley. Dardji et al. (1991) measured fault slip in to northeast – southwest. Cimandiri valley occu- CFZ and resumed that CF is a sinistral strike slip pied by fluviatil deposit composed of boulder, sand, fault and northeast–southwest directions. Martodjojo silt, mud, and clay. On the south of western part of (2003) resumed that CF is a normal fault and part of Cimandiri valley is bordered by Jampang Formation Meratus trend with northeast–southwest directions. which consist of volcanic breccias and lava as a fault Kertapati (2006) said that CF was a normal fault scarp. On the north of eastern part it is covered by type and trending in southwest–northeast direction Quaternary deposits consist of lahar, lava, and ande- sit basalt originated from Pangrango volcano. with component of strike slip which generated de- Landsat and Shuttle Radar Topography Mission structive earthquake along Cimandiri valley. Hall et (SRTM) of Sukabumi area show a lineament along al., (2007) and Clements et al., (2009) suggest that the Cimandiri valley as a CFZ and as seen in yellow [Type text] dash line in Figure 1. This zone aligned in west-east Pinter 1996). If the AF value equal about 50 the tec- direction in the western part and northeast-southwest tonic is relatively stable. In this research we calcu- in the east. late of AF value for 46 drainage basins along the CFZ. The result of AF value ranging from 25,4901 to 74,389. The AF values greater and less than 50 were detected in segment 1, 3 and 4. In segment 2 the AF value near around 50.

Figure 1.The lineament of the Sukabumi area (red lines). The yellow dots represent Cimandiri valley. Several lineaments are also found in northwest- southeast direction and in correlation with segmenta- Figure 3. Map of AF analysis. Numbers show on the tion of CF. We can show that the direction of CFZ map indicates AF value. from the west to the east is not single fault, but seg- mented. 4.2. Hypsometric Curve (HC) According to those facts and field observation, The hypsometric curve describes the distribution CF can be divided into 4 segments. Segment 1 occu- of elevations across an area of land, from one drai- pies on Palabuhanratu and Cibuntu area as shown by nage to the entire planet and can be create by plot- fault scarp, triangular facet hills, fault breccia, slick- ting the proportion of the total basin height and the enside, drag fault, shear and gash fracture, stream total basin area (Keller and Pinter, 1996). The HC offset, and spring water. Segment 2 on can be used as an indicator of a landscape stage in Padabeunghar area with fault scarp, shear and gash the cycle of erosion and divided into 3 stages: fracture and spring water as field evidence. Cikundul young, mature, and old. Active tectonic is indicated and Baros area as Segment 3 with fault scarp, trian- gular facet hills, bulge hill (tilted block hill), fault by young of HC stage. If the HC show the mature breccia, stream deflected, shear and gash fracture and old stage, the erosion process more dominant and spring water. The last segment, Segment 4 lies than tectonic process. In this research, numbers of on Sukaraja area with fault scarp, triangular facet HC measurement sites are 48 drainage basins along hills and spring water were observed in this area. Six the CFZ. The result shows that all segments of Ci- parameters of morphometric analysis used to identi- mandiri Fault are on the young stages and only sev- fy the CF which are drainage basin asymmetry (AF), eral sites at segment 1 indicate mature stage. Mature hypsometric curve (HC), stream length gradient in- stage in segment 1 generally occupies on southern dex (SL), mountain front sinuosity (Smf), valley floor part of Cimandiri valley. width - valleyheight ratio (Vf) and drainage basin (Bs).

Figure 4. Map of HC results. Colour of red, green, blue area indicate young, mature, old stages, respectively. Figure 2.Segmentation of Cimandiri Fault. 4.3. Stream Length Gradient Index (SL) 4.1. Drainage Basin Asymmetry (AF) The stream length gradient index (SL) showed The drainage basin asymmetry was developed in profile valley. The SL is very sensitive to change in the presence of active tectonic deformation and it channel slope by tectonic activity, topography and can detect tectonic tilting at drainage basin scales or rock resistance. The high SL value indicates that val- larger areas. Value of drainage basin asymmetry greater or less than 50 may suggest tilt (Keller and ley profile steeply, deep incision and possible as a

Proceeding of 1st International Seminar of Environmental Geoscience in Asia (ISEGA I), Oktober 2013, page 76 – 83. fault zone and represent tectonic activity (Keller and Pinter, 1996). Lithology along CFZ composed of several rock units (rock formation) from Tertiary to Quaternary age. Segment 1 consists of Quaternary volcanic, fluviatil, breccia of Jampang Formation and calcareous sandstone of Nyalindung Formation. Segment 2 consists of Quaternary volcanic, fluviatil, and calcareous sandstone of Nyalindung Formation. Segment 3 consists of Quaternary volcanic, fluviatil, and breccia of Jampang Formation. Segment 4 con- Figure 6. Map location for Smf analysis. Number indicates sists of Quaternary volcanic. the measurement sites and Smf values are shown in brackets. Number of SL measurement drainage basins sites are 34 along CFZ (Fig.5). The value of SL ranges 4.5 Valley Floor Width-ValleyHeight Ratio (Vf) from 142,47 to 718,8. The SL value greater than 300 Valley Floor Width – Valley Height Ratio (Vf) is found at segment 1, 3 and 4. Meanwhile the value a compare between width and height valley and can which is smaller than 300 found in segment 2. be analyze for tectonic activity. High values of Vf are associated with low uplift rates and the stream cut broad valley floors (Keller and Pinter 1996). Low values of Vfreflecting deep valleys, V shape valleys with stream that are actively incising and as- sociated with uplift. Number of Vf measurement sites are 27 along CFZ. Vf value found in ranging from 0,1856sd 21,6143 (Fig.7). The range value of Vf in segment 1 is 0,7 to 21,6; segment 2 from 1,9 to 8, segment 3 from 0,7 to 3,1 and seg- Figure 5. Map of SL analysis sites ment 4 from 0,2 to 0,8. 4.4 . Mountain Front Sinuosity (Smf) Mountain front is define a topographic transition zone between mountains and plains (Bull, 2009). Mountain front sinuosity is an index that reflects the balance between erosional forces that tend to cut embayment into a mountain front and tectonic forces that tend to produce a straight mountain front coin- cident with an active range bounding fault (Keller and Pinter, 1996). The value of Smf can be detected of tectonic activity. The low value of mountain front Figure 7. Map location for Vf analysis. Number indicates sinuosity is associated with active tectonics and up- the measurement sites and Vf values are shown in brackets. lift and high value is associated with reduces of up- lift and the erosional processes will carve a more ir- 4.6. Drainage Basin Indice (Bs) regular mountain front (Keller and Pinter, 1996). Drainage Basin Indice(Bs) is a comparison the Number of Smf measurement sites are 28 along length and short axis of drainage basin. Bs value can CFZ (Fig.6).The Smf value is ranging from 1,008 to be analyzed for the tectonic activities. The typical 2,58. The average of Smf value in segment 1 on the shape of a basin in tectonically active mountain southern part of Cimandiri Valley smaller than 1,6. range is elongated and becomes progressively more In segment 2 the Smf value varied from 1,2 to 1,9 circular after the cessation of mountain uplift (Bull and dominantly ranging within 1,5 to 1,9. The Smf and Mc Fadden, 1977). Number of Bs measurement sites are 40 along the CFZ and the Bs value ranges value of segment 3 ranges from 1,2 to 2,6 and domi- from 1,3687sd 4,2772 (Fig.8). The average of Bs nantly within 1,2 to 1,5. In segment 4 the Smf value value is 2,2. In general the shape of the drainage ba- is 1. sins is elongated and only on several locations are circular. High value of Bs that higher than average found on eastern part of Cimandiri fault zone (seg- ment 3 and segment 4). In the western part (segment 1) the Bs value generally smaller than the average and only on location 1,2 and 12 Bs value higher than the average one. [Type text]

The result of HC indicated that all segments of CF are young stage, except several locations on segment 1. Western part of segment 1 is a estuary of Cimandiri stream which flow to Palabuhanratu Gulf. Young stage indicated that tectonic force and up- lifted more dominant than erosion process and cha- racterized by rugged relief, deep incision valley and V shape valley. Several locations on segment 1 that mature stage show characterized by undulating mountains relief and U shape valley. The HC indi- Figure 8. Map location for Bs analysis. Number indicates cated that on segment 2, 3, and 4 more active than the measurement sites and Bs values are shown in brackets. segment 1. All segment of CF in general have high of SL 5. Discussion value (SL greater than 300) and characterized by Six morphometric parameters have been calcu- steeply valley, deeply incision and V shape valley. lated to analyze the activity of CF. The AF values In this case reflecting that uplifted by tectonic greater and less than 50 were detected in segment 1, process more dominant than erosion. The SL value 3 and 4. This indicated that occurred of uplift and and profile along Cimandiri valley is reflecting CFZ. tectonic tilting. Drainage basin in this segmen is The SL indicated that all segment is active. elongated. In segment 2 the AF value near around 50 and indicate in this segment less active than segmen 1, 3 and 4.

Hypsometric curve on segment 1 Hypsometric curve on segment 2

1 1 Lokasi 1 Lokasi 25 0,9 0,9 0,8 Lokasi 2 0,8 Lokasi 26 0,7 0,7 0,6 Lokasi 3 0,6 Lokasi 27 0,5 Lokasi 4 0,5 Lokasi 28

y = h/H = y 0,4 y = h/H = y 0,4 0,3 Lokasi 5 Lokasi 29 0,2 0,3 0,1 Lokasi 6 0,2 Lokasi 30 0 0,1 Lokasi 7 0 Lokasi 31 0 0,5 1 Lokasi 8 0 0,5 1 Lokasi 32 x = a/A Lokasi 9 x = a/A Lokasi 33

Figure 9. Hypsometric curve pattern on segment 1. Figure 10. Hypsometric curve pattern on segment 2.

Hypsometric curve on segment 3 Hypsometric curve on segment 4

1 1 0,9 Lokasi 37 0,9 0,8 0,8 0,7 Lokasi 38 0,7 Lokasi 48 0,6 0,6 0,5 Lokasi 39 0,5 Lokasi 49

y = = h/H y 0,4

y = = h/H y 0,4 Lokasi 40 0,3 0,3 Lokasi 50 0,2 Lokasi 41 0,2 0,1 0,1 Lokasi 51 0 Lokasi 42 0 Lokasi 52 0 0,5 1 0 0,5 1 Lokasi 43

x = a/A Lokasi 44 x = a/A

Figure 11. Hypsometric curve pattern on segment 3. Figure 12. Hypsometric curve pattern on segment 4.

Low Smf value found on the mountain front with The different of Vf value can be reflecting of tec- sinuosity relatively straight indicated the presence of tonic activity. In general the Vf value on segment 1, tectonic process. The Smf value of segment 1 in the 3 and 4 dominantly less than segment 2 and charac- southern of Cimandiri valley mean less than 1,6. In terized by deeply valley and V shaped valley. This is segment 2 the Smf value from 1,2 to 1,9. In segment associated by tectonic activity. In segment 2 the val- 3 the Smf value from 1,2 to 2,6 and in segment 4 the ue dominant high (more than 2) and characterized by Smf value is 1. We can conclude based on Smf value U shaped valley. We can conclude based on Vf val- that segment 1, 3 and 4 more active than segment 2. ue that in segment 1, 3 and 4 is more active than segment 2.

Proceeding of 1st International Seminar of Environmental Geoscience in Asia (ISEGA I), Oktober 2013, page 76 – 83. In general the Bs value on segment 3 and 4 more Based on destructive earthquake catalogue of In- than Bs value mean and characterized by elongated donesia, Sukabumi is an area vulnerable to earth- drainage basins shape. This is associated by tectonic quake and several earthquake events is destructively activity. In segment 1 and 2 the Bs value dominat (Supartoyo and Surono, 2008). One case of destruc- less than Bs value mean and characterized by circu- tive earthquake in Sukabumi area occurred on Pebr- lar or rounded drainage basins shape. We can con- uary 10, 1982 with epicenter in land with coordinate clude based on Bs value that all segment is active 7,0º S-106,9º E, magnitude 5,5 Richter Scale, depth and in segment 3 and segment 4 is more active than 25 km and VII Modified Mercally Intensity (MMI) segment 1 and segment 2. intensity scale. The earthquake caused 4 peoples in- Based on result of morphometryparameter calcu- jured, damage building, landslide, and ground frac- late we can classified the tectonic activity level and turing in Cibitung district southern part of Sukabumi showed in this table below. Based on table 1, we city. The epicenter of this earthquake was near the identify tectonic activity level of CF into segment 1, segment 3 and 4 of CF. The earthquake demonstrat- 2, 3 and 4. The result of CF activities showed on ta- ed the CF activities especially on segment 3 and 4. ble 1. The result that the CF on segment 3 and 4 is more active than segmen 1 and 2.

CFZ CFZ

Figure 13. SL profile on segment 1 CFZ. Figure 14. SL profile on segment 2 CFZ.

CFZ CFZ

Figure 15. SL profile on segment 3 CFZ. Figure 16. SL profile on segment 4 CFZ.

Table 1. Summarize of morphometry analyze for identification activity of Cimandiri fault (modified from Bull and Mc Fadden, 1977; Keller and Pinter 1996;).

Morphometry Tectonic Activity Level No. Parameter Less Active Active More Active 1. SL Less than 200 200 to 300 > 300 2. Hc Mature and old stage Young stage Young stage 3. Vf > 3 2 to 3 < 2 4. Bs < 2 2 to 3 > 3 Less than 40 and Less than 30 and 5. AF Around 50 greater than 60 greater than70 6. Smf > 2 1 to 2 < 1 [Type text]

Table 2. The result of morphometry analyze for CF.

Morphometry Cimandiri Fault No. Parameter Segment 1 Segment 2 Segment 3 Segment 4 1. SL Active Active Active Active 2. Hc Less active Active Active Active 3. Vf Less active Less active Active Active 4. Bs Less active Less active Active Active 5. AF Active Less active Active Active 6. Smf Active Less active Active Active

6. Conclusion Kertapati, E.K., 2006, Aktifitas Gempabumi di Indonesia Direction of lineaments along Cimandiri valley is (Perspektif Regional Pada Karakteristik Gempabumi Meru- sak), Pusat Penelitian dan Pengembangan Geologi, ISBN W – E at the western and NE – SW at the eastern- 979-010-X: 109 pp. part. CF can be divided into 4 segments: segment 1, Martodjojo, S., 2003, Evolusicekungan Bogor, Penerbit ITB 2, 3 and 4. The results of morphometric analysis Bandung: 238 pp. suggest that the Cimandiri Fault is an active fault. Noeradi, D., Villemin, T., and Rampnoux, J.P., 1991, Cenozoic Segment 3 and 4 are more active than segment 1 and fault systems and paleostress along the Cimandiri fault zone, West Java, Indonesia, Proceeding of the silver Jubilee Sym- 2. Therefore February 10, 1982 earthquake might be posium, Research and development Center for Geotechnol- closely related to segment 3 and 4. ogy, LIPI, 233-253. Pinter, P., 2005, Applications of tectonic geomorphology for Acknowledgement deciphering active deformation in the Pannonian Basin, Authors thank to Dr. Asep Saepuloh who revis- Hungary, Occasional Papers of the Geological Institute of Hungary, volume 204. ing, improving, and correcting over the manuscript. Soehaimi, A., Kertapati, E.K., dan Setiawan, J.H., 2004, Seis- To Dr. Gede Suantika thank you for discuss about motektonik dan Parameter dasar Teknik Kegempaan Wi- morphotectonic and morphometry. layah Jawa Barat, Lokakarya Cekungan Bandung Geodina- mika, Permasalahan dan Pengembangannya di Bandung References Tanggal 21-22 Desember 2004, Pusat Penelitian dan Abidin, H.Z., Meilano, I., Natawidjaya, D.H., Sarsito, D.A., PengembanganGeologi. Andreas, H., dan Gamal, M., 2008, Studi Karakteristik Soehaimi, A., Sopyan, Y., Marjiyono dan Setianegara, R., Sesar Cimandiri (Jawa Barat) Dengan Metoda Survei GPS 2007, Seismotektonik dan Potensi Kegempaan Wilayah Ja- Untuk Antisipasi Bencana Gempabumi, Laporan Akhir wa, Seminar Sehari Pameran dan Promosi Bidang Geologi Hibah Bersaing Tahun I (2008), Lembaga Penelitian dan di Bandung Tanggal 11 Desember 2007, Pusat Penelitian Pengabdian Pada Masyarakat, ITB. dan Pengembangan Geologi. Bemmelen, R.W., 1949, The geology of Indonesia, Vol. I A., Soekamto, 1975, Peta Geologi Lembar Jampang dan Bale- The Hague Martinus Nijhoff. kambang, Jawa Barat, Pusat Penelitian dan Pengembangan Bull, W.B., and Mc Fadden, L.D., 1977, Tectonic geomorphol- Geologi, Bandung. ogy north and south of the Garlock Fault, Caliornia, In : Supartoyo and Surono, 2008, KatalogGempabumiMerusak In- Doehring (ed.), Geomorphology in Arid regions, Proceed- donesia Tahun 1629 – 2006 (EdisiKeempat), Pusat Vulka- ings of Eight Annual Geomorphology Symposium, State nologi dan Mitigasi Bencana Geologi, Badan Geologi, De- University of New York, Binghampton, p. 115 -138. partemen Energi dan Sumber Daya Mineral: 159 pp. Bull, W.B., 2009, Tectonic geomorphology of mountains : a Suwijanto, 1978, Hubungan antara kegempaan dengan keluru- new approach to paleoseismology, Blackwell publishing : san struktur pada citra landsat di daerah Jawa Barat, Riset, 316 pp. Majalah riset geologi dan pertambangan Jilid 1, No. 2, Ma- Clements, B., Hall, R., Smyth, H.R., and Cottam, M.A., ret 1978, Lembaga Ilmu Pengetahuan Indonesia, 1 – 8. Thrusting of a volcanic arc : a new structural model for Ja- Szynkaruka, E., Monroy, V.,H.,G., and Bocco, G., 2004, Ac- va, Petroleum Geoscience, Vol. 15, 2009, pp. 159 – 174. tive fault systems and tectono-topographic configuration of Effendi, A.C., Kusnama, dan Hermanto, B., 1998, Petageo- the central Trans-Mexican Volcanic Belt, Geomorphology logilembar Bogor, Jawa Barat (edisikedua), Pusat Peneli- 61 (2004), 111–126. tian dan Pengembangan Geologi, Bandung. Verstappen, T.H., 2000, Geomorphological map of Indonesia, Gürbüz, A., and Gürer, O.F., 2008, Tectonic geomorphology of Division of applied Geomorphological surveys, ITC. the North Anatolian Fault Zone in the Lake Sapanca Basin Yeats, R.S., Sieh, K., and Allen, C.R., 1997, The geology of (Eastern Marmara Region, Turkey), Geosciences Journal earthquakes, Oxford university press: 567 pp. Vol. 12, No. 3, p. 215 – 225. Zovoili E., Konstantinidi E. and Koukouvelas I.K, 2004, Tec- Hall, R., Clements B., Smyth H.R., and Cottam M.A., 2007, A tonic geomorphology of escarpment : the cases of Kompo- new interpretation of Java’s structure, Proceedings Indone- tades and NeaAnchialos Fault, Bulletin of the Geological sian Petroleum Association, Thirty-First Annual Convention Society of Greece vol. XXXVI, 2004, 1716 – 1725. and Exhibition, May 2007, IPA07-G-035, CD files. Keller, E.A., and Pinter, N., 1996, Active tectonic earthquake, uplift and landscape, Prentice hall, Upper saddle river, New Jersey 07458: 338 pp.

Proceeding of 1st International Seminar of Environmental Geoscience in Asia (ISEGA I), Oktober 2013, page 76 – 83.