World Journal of Engineering and Technology, 2014, 2, 61-70
Published Online September 2014 in SciRes. http://www.scirp.org/journal/wjet
How to cite this paper: Nurwihastuti, D. W., Sartohadi, J., Mardiatno, D., Nehren, U. and Restu (2014) Understanding of
Earthquake Damage Pattern through Geomorphological Approach: A Case Study of 2006 Earthquake in Bantul, Yogyakarta,
Indonesia. World Journal of Engineering and Technology, 2, 61-70. http://dx.doi.org/10.4236/wjet.2014.23B010
Understanding of Earthquake Damage
Pattern through Geomorphological
Approach: A Case Study of 2006
Earthquake in Bantul, Yogyakarta,
Dwi Wahyuni Nurwihastuti1, Junun Sartohadi2, Djati Mardiatno2, Udo Nehren3, Restu1
1Department of Geography, State University of Medan, Medan, Indonesia
2Faculty of Geography, Gadjah Mada University, Yogyakarta, Indonesia
3Institute for Technology and Resources Management in the Tropics and Subtropics, Cologne University of
Aplied Sciences, Cologne, Germany
Received May 2014
The last major earthquake in Bantul causing severe damage occurred on May 27th, 2006. The dam-
ages in the flat area of Bantul had a certain pattern. The d am ag es pattern controlled the subsur-
face characteristic below the flat area. Understanding earthquake damage pattern through geo-
morphological approach is important for earthquake hazard analysis. The techniques of remote
sensing and Geographical Information Systems were applied to analyze earthquake damage pat-
tern and geomorphological characteristics. Gravity analysis was used to identify the subsurface
structure and the basement depth while geoelectric analysis was used to identify sediment depth.
Moreover, spatial correlation analysis was used to identify the relationship between the earth-
quake damage, geomorphological characteristics, and subsurface characteristics. The results
show that fluvial, marine, and aeolian landforms have low rock density value based on gravity
analysis. These indicate that they were composed by thick unconsolidated material of quaternary
alluvium. While denudational, structural, and solutional landforms composed by material of ter-
tiary rocks have high rock density value. The severe damage occurred in the area that has a lower
value of local gravity and deeper basement. In contrast, the slight damage occurred in the area
that has higher values of local gravity and shallower basement. Moreover, the severe damage oc-
curred in areas of thicker sediment that consist of unconsolidated material. Consequently, the
area of unconsolidated material that has deeper basement and thicker sediment is prone to
earthquake. They were located on fluvial, marine, and aeolian landforms.
Earthquake Damage Pattern, Geomorphology, Subsurface Characteristic
D. W. Nurwihastuti et al.
Indonesia has a lot of earthquakes because the Indonesian Archipelago is a result of the collision of three main
tectonic plates: 1) the Eurasian plate, 2) the Indian Ocean—Australian plate, and 3) the oceanic West Pacific
plate . Minster and Jordan (1978) in (Verstappen, 2000)  described that the Southeast Asian plate moves 1
cm/ye ar s out h—eastward, the Indian Ocean—Australian plate 7 cm/year northward and the West Pacific plate 9
cm/year westward. Moreover, the Indian Ocean—Australian plate subducts at a rate of 6 - 7 cm/year beneath
Sumatra and Java Islands as parts of the Eurasian plate -. This convergent plate boundary dominates tec-
tonic and volcanic processes as subduction zones. Consequently, the collision of those three major tectonic
plates affects Indonesia that is located in a very active earthquake region.
The Indonesian earthquake created serious damage in many places in Java, e.g. the Bantul earthquake that
happened in Java Island on May 27th, 2006. Bantul is located in Yogyakarta Special Province, Java Island, In-
donesia, as presented in Figure 1. The 2006 earthquake in Bantul caused severe da mage. The earthquake dam-
age pattern is unique in the flat ar ea of Bantul. T he damage pattern is relate d to the patter n of sediment thickness,
while the surface of the alluvial plain looks homogenous. Identification of subsurface condition through detail
surface characterization is becoming a challenge. This study aims to get a better understanding of the earthquake
damage pattern and the correlation with the subsurface characteristics, which is of utmost importance for earth-
quake hazard prediction as well as land use and settlement planning.
Some techniques of remote sensing and Geographical Information Systems were applied to analyze earthquake
damage pattern and geomorphological characteristic. The earthquake damage pattern was obtained from visual
interpretation of IKONOS after 2006 earthquake and secondary data of damage. The geomorphological charac-
teristic was obta ined from visual interp retation o f ASTER and field observatio n. Furthermore, geophysica l tech-
niques were applied to analyze subsurface characteristics, i.e. geoelectric and gravity analyses. Geoelectric
analysis was applied to obtain sediment thickness and material type. It was supported by drilling data. Gravity
analysis applied Bouguer Anomaly Map to identify the subsurface structure and the basement depth. The first
step is the conversion from Bouguer Anomaly Map to digital data. The digital data of Bouguer Anomaly must
be projected onto flat areas. The next step is separation of local anomaly and regional anomaly using upward
continuation. The local anomaly and geological information were applied to make subsurface modeling. This
step produces subsurface structure. Moreover, spatial correlation analysis was used to identify the relationship
between the earthquake damage, geomorphological characteristics, and subsurface characteristics.
Figure 1 . Bantul is located in Y ogyakarta Special Province, Java Island, Indo nesia.
D. W. Nurwihastuti et al.
3. Results and Discussion
3.1. Earthquake Damage Pattern of Bantul
The 2006 earthquake in Bantul caused a lot of damage. According to International Recovery Platform (IRP)
(2009)  and Bappenas (2006) , more than 1.1 million people in the provinces of Yogyakarta and Central
Java were affected by this earthquake. The victim indicated 5716 confirmed deaths and 37,927 survivors with
severe injuries. The damage was very heavily concentrated on the housing sector with 52.48% damages.
Bantul area is the most destroyed areas due to 2006 earthquake. According to Pemerintah Provinsi DIY &
Pemerintah Provinsi Jawa Tengah (2006) and Pemerintah Provinsi DIY (2006) , the victims are 223,117
households which consist of 779,287 people with 4143 people dead. Furthermore, the houses damaged are
71,763 collapses, 71,372 heavily damaged and 73,669 slightly damaged. Consequently, the Bantul area is earth-
quake prone areas.
The areas of damage due to 2006 earthquake were covered Yogyakarta Province and part of Central Java
Province. Bantul is the most severe damage and many casualties. The damage occurred in the plains area. Ac-
cording to Yamazaki and Matsuoka (2007) , Subdistrict of Pundong, Bambanglipuro, Jetis, and Pleret is an
area that has the highest ratio of house damage (75% - 100%), while Piyungan Subdistrict having 50% - 75%
damage ratio. Subd istrict o f Imogi ri , S e won, B antul, P aj anga n, a nd B ang un ta pa n su f fer e d d amage r at io o f 25 % -
50%, while Subdistrict of Dlingo, Sedayu, Kasihan, Kretek, Sanden, Srandakan, and Pandak suffered only
damage ratios from 12.5% - 25%. In additional, the intensive damage zone extends for 1 8 km i n the North-So ut h
direction along Subdistrict of Pleret, Jetis, and Pundong with total collapse rate over 60% and the human loss
rate over 1.6% .
The detail spatial distribution of damage due to 2006 earthquake is focused in Bantul Lowland. The damage
only focuses on the settlement area. The criteria of damage based on classification of building damage as quali-
tatively. There are 3 classes of damage, i.e. severely damage, moderately damage, and slightly damage. The
damage was determined based on interpretation of IKONOS imagery, secondary data, and field check. The
earthquake occurred on 27 May 2006, so field checks used interviews with community and identify the former
damage and the residual damage. Table 1 provides the percentage of earthquake damage in Bantul District.
Figure 2 illustrates the detail spatial d istr ibution of damage in Bantul District.
3.2. Geomorphological Characteristics
Geomorphological characteristics cover geomorphological aspects and landform. Geomorphological aspects
consist of morphology, morphogenesis, morphochronology and morphoarrangement . Morphology in Bantul
was interpreted based on digital elevation models (DEM) of SRTM (Shuttle Radar T opographic Mapping Mis-
sion) . SRT M data are useful for large geographic areas [11 ], such as B a nt ul. T he el evati on o f B antul has a r a ng e
from 0 m to 507 m above mean sea level. The low point had been located at along the coastline of the Bantul
coastal area. While the highest point is located at the Bat uragung Ra nge, i.e. Sudi moro M ountain i n Man gunan
Village, Dlin go Sub D istrict. The morphology o f B a ntul can be cla ssified in plain, hill, and mo unta in.
The process of landform composing is closely connected to the genesis or morphogenesis. Genesis is the
Greek word for origin or creation and in geomorphology the term relates to the origin of a landform, in other
words the process responsible for the creation of the form . Thus, morphogenesis is the geomorphological
aspect that related to the origin and development of landform. Morphogenesis can be detailed into passive mor-
phostructure, active morphostructure, and morphodynamic. Passive morphostructure is related to lithology, both
rock types and structures while the active morphostructure is related to endogenous dynamics that contain tec-
tonic events during the l andfo rm fo rmati on. The pa s sive morphostructure t hat was found in the Ba ntul are faults,
lineaments, escarpments and anticline. The passive and active morphostructure of Bantul is presented in the sur -
face lithological map. Morphodynamic is rela ted to exogenous d ynamics. Morp hodyna mic of B antul is c aused
by water and wind that consist of several types. There are mass movements including soil e rosion, sedimenta-
tion caused by water and sand deposits caused by wind. Mass movements including soil erosion were oc-
curred in the hills and mountain areas in Bantul. Sedimentation was occurring along rivers in Bantul, espe-
cially the main river, i.e. Progo River and Opak River. The sand deposits caused by wind were occurring along
coastal areas in Bantul.
Morphochronology is describing absolute and relative dating of landforms and related processes. Morphoch-
ronology in the Bantul area was analyzed refers to the relative dating of landforms and related processes, e.g.
D. W. Nurwihastuti et al.
Table 1. Th e percent age of earth quake damage i n Bantul.
Damage Corresponding Areas Are a
1 Sligh tly All area of Kasihan, Pajangan, Kretek, Srandakan, Sanden, Sedayu, and Dlingo
Hill an d mountain area of Piyungan, Pleret, Imogi ri, and Pundong Subdistrict 331.20 6 0.37
2 Mod era tely All area of Pandak Subdistrict 24.47 4.75
3 Sever el y All area of S ewon, J etis, Banguntapan, Bantul, and Bamba nglipu r o Subdistrict
Plain area of Piyungan, P leret , Imogiri, and Pu ndong Subdistrict 179 .82 34. 88
Total Area of Bantul 515.49 100 .00
Source: Data analysis result (2013)
Figure 2. The detail spatial distribution of damage in Bantul District.
you n g beach ridge and old beach ridge. The young beach ridge was created after the old beach ridge. The land-
forms that located close to the coast are the younger landforms, because of the active processes of wave in the
coast. Furthermore, the landforms that located close to the river are the younger landforms, because of the active
processes of water flow in the r iver. In a ddition, mor phochr onolo gy is also de scribing t he genes is of eac h land-
Morphoarrangement is describing the spatial arrangements and interrelationships of various landforms and
processes. Hilly and mountain areas can be divided into peak, upper slope, middle slope, lower slope and foot
slope plain based on morphoarrangement. Alluvial plains also can be divided into natural levee and flood plain
based on morphoarrangement. Natural levees were located along river and they have more higher relief compare
D. W. Nurwihastuti et al.
the surrounding areas. Flood plains were located in the back of the natural levees that have lower relief compare
the surrounding areas. The general landforms of the Bantul area consist of 6 landforms based on their genesis.
They are fluvial landform, marin landform, aeolian landform, solutional landform, denudational landform and
structural landform. Moreover, there are 48 detail landforms.
3.3. Subsurface Characteristics
Sunsurface characteristics in this study cover lithological characteristics, paleo-sedimentation processe, and
schematic past relie f pa tte rn in Ba ntul. Stratigraphically, the litho logy of B antul from olde r to younger c onsist o f
Semilir Formation (Tmse), Nglanggran Formation (Tmn), Sambipitu Formation (Tms), Sentolo Formation
(Tmps), Wonosari Formation (Tmwl) and Quaternary deposits. Generally, Bantul was composed by two litho-
logical controls that were very different, i.e. Quaternary deposits and Tertiary rocks. Quaternary deposits were
composed of sand deposits as a product of Merapi Volcano and clay deposits as a result of Tertiary rock wea-
thering. While the Tertiary rocks was divided into Tertiary igneous rocks and Tertiary sedimentary rocks.
Moreover, Tertiary igneous rocks were composed by Semilir Formation, Nglanggran Formation and Sambipitu
Formation. Otherwise, the Tertiary sedimentary rocks were composed by Wonosari Formation and Sentolo
Semilir Formation consists of interbedded tuff-breccia, pumice breccia, dacite tuff, andesite tuff and tuffa-
ceous claystone of Upper Oligocene—Lower Miocene. Nglanggran Formation consists of volcanic breccia, flow
breccia, agglomerate, lava and tuff of Lower Miocene. In addition, Smyth et al. (2005; 2008)   ment ion
the Semilir and Nglanggran Formations form part of sequence of volcanic and volcaniclastic rocks that are
exposed over a large area. They were deposited in a very short time period, at most about one million years.
Furthermore, S myt h et al. (2008) [14 ] mention that Semilir eruption oc c urred in Lower Miocene.
Sambipitu Formation consists of tuff, shale, siltstone, sandstone and conglomerate of Middle Miocene. Wo-
nosari Formation consists of coral reef limestone, calcarenite and tuffaceous calcarenite of Upper Miocene—
Upper Pliocene. Sentolo Formation consists of limestone and marly sandstone of Middle Miocene—Upper Pli-
oce ne. It sp reads a long the l ow hills surro unding P rogo River , in the western a nd east ern of P rogo Rive r. Mo re-
over, McDonald and Partners (1984)  divided Sentolo Formation into 3 kinds, na mel y Sentolo -1, Se ntolo-2
and Se ntol o-3. T he Sento lo-1 consists of marls, tuffs and conglomerates. The Sentolo-2 consists of marly li mes-
tones and calcarenites. The Sentolo-3 consists of bedded limestones.
The structure of Bantul and its surrounding are strongly influenced by plate tectonic movement between the
Eura sia n pla te and the Indi an -Australian plate. Bantul is a part of Yogyakarta Basin. The geological structure of
Yogyakarta Basin is a graben. It confined by two faults, Progo River fault on the west and Opak River fault
bordered Southern Mountains to the east. These faults were interpreted from the gravity pattern . The Yo-
gyakarta Basin is mostly covered by Young Merapi sediments that consist of tuff, volcanic ash, breccias, ag-
glo merate and lava of Quater nary age . T he thickness of the sediment is up to 100 m . The other sedi-
ments are river and coastal sediments. River and coastal sediments consist of gravel, sand, silt and clay of Holo-
cene age . Fa ul t syst em in thi s area is interpreted as a buried fault  .
Paleo-sedimentation is a sedimentation that occurred at the past time. Paleo-sedimentatio n in Bantul Lo wland
can be identified based on material of sedimentation result. The material of sedimentation contained information
about earth surface environments in the past. The material of sedimentation result can be identified based on
geoelectric data and drilling data.
The geoelectric data provide the resistivity of constituent material of Bantul area. Based on the resistivity
values, it can know the constituent material of Bantul area. In order to obtain the kind of materials, it is neces-
sary the geological map to support interpretation of geoelectric data.
Based on the geoelectric analysis, it can know that the material of Bantul Lowland was covered by alluvium.
It proved that fluvial processes have been working in this area. The fluvial processes consist of transportation
and sedimentation. The thickness of alluvium reached 150 m based on the geoelectric analysis. This thick allu-
vium indicates that the sedimentation occurs repeatedly. The geoelectric analysis results can be confirmed by the
analysis of dr illing data.
The re a re 52 po ints o f dri llin g d ata thr ougho ut B antu l Lo wla nd. T he d epths va r y fro m 20 m to 150 m. Gener-
ally, the composition of the sediment is unconsolidated material that derived from Merapi Volcano. They consist
of sand, gravel, clay, and silt. In some borehole data, there are breccias layers. They proved that the material de-
D. W. Nurwihastuti et al.
rived from fluvial processes. It is characterized by repetition of sand units that were dominant with grain size
from fine to coarse: silt, clay, in some places the sand-gravel mixture and breccias. The repetition layers such as
these show that the areas have been repetitive sedimentation process caused by lifting and decline both by tec-
tonic processes and by past sedimentation in the Bantul basin.
Past relief showed the relief in an area in the past. The past relief is reflected based on the basement of Bantul
Lo wla nd which consists of Tertiary materials. The basement of Bantul Lowland has been analyzed using gravity
information that used as a way to predict the geological structure and the density of the rocks making up the
Earth’s crust. According to Widijono and Subagio (2009) , gravity anomaly distribution plays an important
role to determine the distribution of rocks and geological structures below the surface that is covered by Qua-
ternary sediments. Widijono and Subagio (2009)  also stated that the straightness of Bouguer anomaly is
thou ght to be a resp onse to the gravi ty o f the re giona l st ruct ura l linea me nt. M ore over , b ased o n the c onto ur map
of gra vity also can be derived basement depths  . T he highs and lo ws i n the B ougue r gravity anomalies
were interpreted as basement highs and lows .
The gravity analysis applied Bouguer Anomaly Map of The Yogyakarta Quadrangle Java by Marzuki and
Otong (1991)  which was published by Geological Research and Development Centre, Directorate General
Geology and Mineral Resources, Department of Mines Energy. Bouguer anomaly map is a gravity anomaly map
that reflects the spreading pattern of rock density.
The Bouguer Anomaly map was analyzed to get the local or residual gravity anomaly map. The analysis is
performed in Yogyakarta, Bantul and the surrounding area. The values of local gravit y anomaly in Yo gya kart a
and its s urroundin g area are varied from −12.9 mGal up to +15.9 mGal as presented in Figure 3.
The value of local gravity anomaly was interpreted to know subsurface structure. The striking differences in
local gravity anomaly value and t he st raightness of local gravity anomaly reflec t any fa ult in that area. The nega-
tive value of local gravity anomaly indicated that the area has low rock density. The low rock density indicated
Figure 3 . The local or the residual gravity anomaly of Yogyakarta and its surrounding area.
Cross section AB
Cross section CD
D. W. Nurwihastuti et al.
that the area consists of unconsolidated material. On the other hand, the positive value of local gravity anomaly
indicated that the area has higher rock density. The higher rock density indicated that the area consists of Ter-
tiary sediments and Tertiary rocks.
There are 3 kinds of rocks based on the rock density in Yogyakarta, Bantul and the surrounding area. They are
unconsolidated material, Tertiary sediments (limestone) and Tertiary rocks (igneous rocks). The rock density of
unconsolidated material is 2.0 - 2.27 g/cm3. The rock d ensity of T ertia ry sediments ( limes tone) is 2 .5 g/cm3. The
rock density of Tertiary rocks (igneous rocks) is 2.73 - 2.80 g/cm3. Based on the subsurface modeling, it indi-
cated that there is a buried fault between Yogyakarta and Bantul and a graben structure in Bantul area.
Based on the cross section of subsurface modeling in the some part of Bantul Lowland, it can be interpreted
that the geological structure of Bantul is asymmetry graben. The eastern part of graben is deeper than the west -
ern part of graben. The basement depth of graben varies up to 1.6 km. These results are consistent with studies
of Fukuoka et al. (2008) , Setijadji et al. (2008) , and Daryono (2011) . Bantul Lowland is a p art of
Yogyakarta Basin. Fukuoka et a l. (2008 )  have been del ineated t he density str uctur e of the Yo gyakar ta Ba-
sin. T he r esult sho ws tha t the r e is 3 0 - 40 km wide a nd more than 2 km de ep grab en str uct ure in t he Y ogya kart a
Basin. According to Setijadji et al. (2008) , Yogyakarta Basin is a half-graben structures that deeper at its
eastern margin. Moreover, Daryono (2011)  stated that resonance frequency data of microtremor measure-
ments can describe the profiles of graben bedrock depth qualitative, so it is known that the B antul Grab en is no t
a symmetrical graben type with the bedrock more depth in the eastern.
The past relief pattern in Bantul Lowland now was covered by sediment material. The sediment depth of
Bantul Lowland can be identified from drilling data and geoelectric data. Based on the analysis of drilling data
and geoelectric data, it can conclude the sediment in the Bantul area varied from 3 m up to 150 m. The deepest
sediment conducts in the eastern part of Bantul Lowland. The deeper sediment is close to the escarpment of Ba-
turagung Ra nge. While t he shallo wer sedime nt close to Se ntolo hill a nd Sentolo i solated hill. T his fact ind icates
that the basement of Bantul Lowland is not flat but sloping and irregular. The deeper basement occurred in the
eastern part. Otherwise, the shallower basement occurred in the western part.
3.4. Correlation of Earthquake Damage Pattern, Geomorphological Characteristic and
The severely damage due to 2006 earthquake occurred in area of fluvial landform. The spatial correlation be-
tween earthquake damage pattern and subsurface characteristic was divided into the spatial correlation between:
earthquake damage pattern and basement depth, earthquake damage pattern and sediment thickness, earthquake
damage pattern and material type. The results of spatial correlation between earthquake damage pattern and
subsurface characteristics were described as follows:
1) Generally, the severely damage occurred in the area that have a lower value of local gravity and deeper
base ment . In c ontr ast, the s lig htl y dama ge o ccur red in the ar ea tha t ha ve hi gher val ues of loc al gr avit y and s hal -
lower base ment.
2) The severely damage occurred in areas of thicker sediment. Based on statistical analysis of Spearman rank
correla tion, the correlation coefficient between earthquake damage pattern and sediment thickness is 0.707
(str o ng co r re la tio n) . I t mea ns t he th ic ke r se d i men t t he mo r e d ama ge. O n t he o t he r hand , t he thi nne r sed i me nt the
3) The severely damage occurred in area of unconsolidated material. This fact indicates that the area of un-
consolidated material is prone to earthquake.
The results of spatial correlation between earthquake damage pattern and sediment thickness are accordance
with the research result of Naing (2010)  and Karnawati et al. (2008) . Accord ing to N aing (2010) ,
the thick sediment area has strong effects on amplification characteristics and high amplification zones relatively
coincide with high damage areas during the 2006 earthquake. Additionally, Karnawati et a l. (2008)  mention
that the most susceptible zone o f earthquake was the area which consists of the thickest sediment.
Moreover, the results of spatial correlation between earthquake damage pattern and material type indicate that
the area of unconsolidated material is prone to earthquake. On the other hand, the area of consolidated material
is the area of earthquake safety. According to Karnawati et al. (2008) , the most susceptible zone of the
earthquake was the area in Bantul which consist of the loosest gravelly sand—silty sand of Recent Opak—Oya
River d eposits. Fukuoka et al. (2008)  also mention that the damaged area due to 2006 earthquake occurred
in Bantul area that consists of unconsolidated soil. While, Walter et al. (2008)  mention that earthqua ke
D. W. Nurwihastuti et al.
Figure 4. A Cro s s s ection s hows the corr elation bet ween ear thquake damage pattern an d subsu rface characteristics.
damage occupied in an area of weak sediments. In the other case, Sato et al. (2004)  state that the severely
damage due to 2003 Colima (Mexico) earthquake occurred in plain areas that consist of soft sediment. Moreover,
Pidwirny (2009)  mentions that unconsolidated materials have a tendency to increase the amplitude and du-
ration of the seismic waves increasing the potential for damage. Figure 4 illustrates a cross section shows the
correlation between earthquake damage and subsurface characteristics in Bantul.
There are correlation between earthquake damage pattern, geomorphological characteristic, and subsurface cha-
racteristic. The severe damages occurred in area that has deep basement, low gravity anomaly, thick sediment,
and unco nsol idated mater i al. On the other ha nd, the slig ht damages occurred in area that have shallow basement,
high gravity anomaly, thin sediment, and consolidated material. They are located on fluvial landform.
 V erstap p en, H.Th . (2000 ) Outline of the Geomorphology of Indonesia: A Case Study on Tropical Geomorphology of a
Techtogen e R egi on. ITC P ublication, Number 79, Enschede.
 Tregoning, P., Brunner, F.K., Bock, Y., Puntodewo, S.S.O., McCaffrey, R., Genrich, J.F., Calais, E., Rais, J. and Sub-
arya, C. (1994) First Geodetic Measurement of Convergence across the Java Trench. Geophysical Research Letters, 21,
 McCaffrey, R. (1996) Asia Slip Partitioning at Convergent Plate Boundaries of SE. Geological Society, London ,
Special Public atio ns , No. 106, 3-18. http://dx.doi.org/10.1144/GSL.SP.1996.106.01.02
 Kato, T., Ito, T., Abidin, H.Z. and Agustan (2007) Preliminary Report on Crustal Deformation Surveys and Tsunami
Measurements Caused by the July 17, 2006 South off Java Island Earthquake and Tsunami, Indonesia. Earth Planets
Space, 59, 1055-1059 . http://dx.doi.org/10.1186/BF03352046
 International Recovery Platform (2009) The Yogyakarta and Central Java Earthquake 2006. Recovery Status Report,
 Bappenas (2006) Preliminary Damage and Loss Assessment, Yogyakarta and Central Java Natural Disaster: A Joint
Report o f BAP PEN AS, the Provincial and Local Govern ments of D. I. Yogyakarta, the Provincial and Local Govern-
ments of Central Java, and In ter natio n al P art ner s. Th e 15th Meeting of the Consultative Group on Indonesia (CGI) Ja-
karta, 14 June 2006, Jakarta, 140 p .
 Pemerintah Provinsi DIY & Pemerintah Provinsi Jawa Tengah (2006) ATLAS Kawasan Gempa Bumi 27 Mei 2006.
D. W. Nurwihastuti et al.
Pemerin tah Provinsi DIY dan Pemerintah Pro vinsi Jawa Tengah, Y ogyakarta.
 Yamazaki, F. and Matsuoka, M. (2012) Remote Sensing Tools for Earthquake Response and Recovery. International
Symposium on Remote Sensing Applications to Natural Hazards.
 M ura kami , H. , P ramitasari, D. and O hno, R. (2008) Huma n Casualty and Damage Distribution in Relation to Seismic
Intensity in The 2006 Central Java Earthquake in Indonesia. The 14th World Conference on Earthquake Engineering,
12-17 October 2008, Beijing.
 Van Zuidam, R.A. (1985) Aerial Photo-Interpretation Terrain Analysis and Geomorphology Mapping. Smits Pub-
lisher s, The Hague, 442 p.
 Bishop, M.P., James, L.A., Shroder Jr., J.F. and Wal sh , S.J. (2012 ) Geospatial Technologies and Digital Geomor-
phological Mapping: Concepts, Issues and Research. Geomorphology, 137 , 5-26.
 Gustavsson, M. (2005) Development of a Detailed Geomorphological Mapping System and GIS Geodatabase in
Sweden, Chapter s 1-4: Review of Geomorphological Mapping. Licentiate Thesis, May 2005.
 S m yth , H., Hall, R., Hamilton, J. and Kinny, P. (20 05) East Java: Cenozoic Bas in s, Volcanoes and Ancient Basement,
Proceedings, Ind ones ian Petroleum Association, Thirtieth Annual Convention & Exhibition, August 2005.
 Smyth, H.R., Hall, R. and Nichols, G.J. (2008) Cenozoic Volcanic Arc History of East Java, Indonesia: The Stra-
tigraphic Record of Eruptions on an Active Continental Margin . In Draut, A.E., Clift, P.D. and Scholl, D.W., Eds.,
Formation and Applications of the Sedimentary Record in Arc Collision Zones: Geological Society of America Sp ecial
Paper 436, 199-222.
 McDonald and Partners (1984) Greather Yogyakarta Groundwater Resources Study, Volume 3: Groundwater: Gov-
ernment of the Republic Indonesia, Ministry of Public Works, Directorate General of Groundwater Resources Devel-
opment Groundwater, Development Project (P2AT).
 Untung, M., Udjang, K. and Ruswandi, E. (19 73) Gayaberat di daerah Yogyakarta, Wonosari, Jawa Tengah (Gravity
Survey in th e Yogyakarta, Won osari Area, C entral Java) , Geological Survey of Ind onesia. Publikasi Teknik seri Geofi-
sika, No. 3, 7 h.
 van Bemmelen, R.W. (1970) The Geology of Indonesia. 2 nd Edi tion, Martinus Nijhoff, The Hague.
 Pramumijoyo, S. and Sudarno, I. (2008) Surface Cracking Due to Yogyakarta Earthquake 2006. In: Karnawati, D.,
Pramumijoyo, S., Anderson, R. and Husein, S., Eds., The Yogyakarta Earthquake of May 27, 2006, Star Publisher, Los
Angeles (in Press).
 Rahardjo, W., Sukandarrumidi and Rosidi, H.M.D. (1995) Geological Map of the Yogyakarta Sheet, Jawa, Scale
1:100.000. Geological Research and Devel opment Centre, B andung.
 Widijono, B.S., dan Subagio (2009) Anomali Gaya Berat Sebagai Salah Satu Petunjuk Keterdapatan Gejala Struktur
Geologi Daerah Jogjakart a dan sekitarn ya, Prosiding Workshop Geologi Pegunungan Selatan 2007, Pub likasi Khusu s
No. 38, ISBN 978-979-551 -019 -2, Pusat Survei Geologi, Departemen Energi dan Sumber Daya Mineral Bandung, In-
 Barros, L.V. and Assumpcao, M. (2011) Basement Depths in the Parecis Basin (Amazon) with Receiver Functions
fro m Small Lo cal Ear thq u akes in the Porto Dos Gaúchos Seismic Zon e. Journal of South American Earth Sciences, 32,
 Marzuki and Otong (19 91) Bouguer Anomaly Map of The Yogyakarta Quadrangle Java, Geologi cal Research and De-
velopment Centre, D irector ate General Geol ogy and Mineral Resources, Dep ar tment o f Mines Energy.
 Fukuoka, K., Ehara, S., Fujimitsu, Y., Udi, H., Setyawan, A., Setijadji, L.D., Harijoko, A., Pramumijoyo, S., Setiadi, Y.
and Wahyudi (2008) Interpretation of the 27 May 2006 Yogyakarta Earthquake Hypocenter and Subsurface Structure
Deduced from the Aftershock and Gravity Data. In: Karnawati, D., Pramumijoyo, S., Anderson, R. and Husein, S.,
Eds., The Yogyakarta Earthquake of May 27, 2006, Star Publ is he r , Los A nge l e s (in Press).
 Setijadji, L.D., Watanabe, K., Barianto, D.H., Rahardjo, W., Sudarno, I., Susilo, A. and Itaya, T. (2008) Sear ching for
the Active Fau lt of the Yogyakart a Earth quake of 2006 Using Data Integration on Aftershocks, Cenozoic Geo-History,
and Tectonic Geomorphology. In: Karnawati, D., Pramumijoyo, S., Anderson, R. and Husein , S., Eds. , The Yogyakarta
Earthquake of May 27, 2006, Star Publisher, Los Angeles (in Press).
 Daryono (2011) Indeks Kerentanan Seismik berdas arkan M ikrotremor pada S etiap Satuan B entuklahan di Zona Graben
Bantul Daerah Istimewa Yogyakarta, Disertasi, Program Pascasarjana Fakultas Geografi, Universitas Gadjah Mada,
 Naing, T. (2010) Analysis of Microtremors for Site Amplification Characteristics and Ground Motion in Yogyakar ta,
Indonesia, Dissertation, Faculty of Engineering, Gadjah Mada Un iversit y.
D. W. Nurwihastuti et al.
 Karnawati, D., Husein, S., Pramumijoyo, S., Ratdomopurbo, A., Watanabe, K. and Anderson, R. (2008) Earthquake
Microzonation and Hazard Maps of the Bantul Area, Yogyakarta, Indonesia. In Karnawati, D., Pramumijo yo, S., An-
derson, R. and Husein, S., Eds ., The Yogyakarta Earthquake of May 2 7, 2 006 . Star Publish er , Los Angeles (in Press).
 Walter, T.R., Luehr, B.G., Wang, R., Sobiesiak, M., Grosser, H., Wetzel, H.U., Milkereit, C., Zschau, J., Wassermann,
J., Harjadi, P. and Brotopuspito, K.S. (2008) The 26 May 2006 6.4 Yogyakarta Earthquake South of Mt. Merapi Vol-
cano: Did Lahar Deposits Amplify Ground Shaking and thus Lead to Disaster? Geochemistry, Geophysics, Geosys-
tems. An Electronic Journal of the Earth System. http://www.volcanotectonics.de/publications.html
 Sato, T., Nakamura, Y. and Saita, J. (2004) Evaluation of The Amplification Characteristics of Subsurface Using Mi-
crotremor and Strong Motion: The Studies at Mexico City. 13th World Conference on Earthquake Engineering, P aper
No. 862, Va ncouve r, BC, Canada.
 Pidwirny, M. (2010) Earthquakes. Fundamentals of Physical Geography. 2nd Edi tion.