INTRODUCTION
Landslides are dangerous natural hazards that take heavy tolls on human lives and properties. Landslides often occur in tropical countries such as Malaysia. It is one of the main constraints for development projects in the highlands of the country. Most of these landslides are shallow rainfallinduced landslides that normally occur in steep hilly areas and highlands as an aftermath of heavy rainfall during monsoon season.
However, the risk of landslide incidents could possibly be minimized if the
knowledge of the potentially landslide prone areas are known in prior. Generally,
the prediction of occurrence of a potentially landslides in future is represented
in the form of landslide susceptibility map. Landslide hazard mapping is essential
for land use activities and management (Moghaddam et
al., 2007). Varnes (1984) indicates that the
occurrences of landslide hazard can be evaluated based on the possibility of
incidence of this conceivably ruining phenomenon within a particular period
of time and within a given area. These early timely indication maps of slope
stability prone areas are mandatory tools for various experts such as engineers,
geologists, planners and decision makers. These susceptibility maps will help
in selecting the appropriate sites for development of agriculture, construction
and many other activities.
The Geographical Information Systems (GIS), enables data acquisition, storage, retrieval, modeling and manipulation. The GIS systems have the capability to incorporate various geographical technologies including remote sensing and global positioning systems hence, they have become very vital for landslide susceptibility mapping. The analytical and combinational capacity of GIS has enabled the production of techniques used in landslide assessment for generating more precise maps, detailing the probable landslide hazard prone areas.
Landslide susceptibility mapping can vary from simple methods that use a minimum
data to sophisticated mathematical methods that use practical mathematical methods
using complex databases in computerbased Geographic Information System (GIS).
For assessing landslide hazard different methodologies are proposed which are
mainly grouped as: qualitative and quantitative methods. Qualitative approaches
are based on the sitespecific experience of experts and the susceptibility/hazard
areas are determined directly in the field or by combining different index maps.
Whereas, quantitative methods calculate susceptibility/hazard probability based
on the numerical expressions of the relationship between causative factors and
landslides (Solaimani et al., 2009). The two
main types of quantitative methods are deterministic and statistical (Aleotti
and Chowdhury, 1999). The deterministic models are physically based models
which are used only to assess and examine the slope stability for small areas
due to the need of comprehensive geotechnical data. Hence, statistical methods
in landslide evaluation are generally used in large areas. In statistical methods,
the role of all the factors that cause landslides is defined based on the computed
associations between those factors and landslide distributions. They are based
on a general theory which claims that, the landslides in the future will be
more likely to occur, due to the existence of the same conditions that have
caused landslides in the past.
In this study, landslidehazardous areas are analyzed and mapped using the
landslideoccurrence factors through the heuristic approach named Analytic Hierarchy
Process (AHP). This GISbased AHP method has been applied in previous studies
which has proved to be very effective and valuable method to landslide susceptibility
mapping (Ercanoglu et al., 2008; Yalcin,
2008).
MATERIALS AND METHODS
Study area: The study area lies in the central northern part of Peninsular Malaysia along the EW highway between 5°:24":6' N to 5°:45":56.5' N latitude and 101°:7":53.6' E to 101°:50":26' E longitude, with a total area of 1205 km^{2} (Fig. 1). It is characterized by rugged hills and mountainous terrain covered by thick rain forest. The study area is frequently subjected to landslides following heavy rains, especially, alongside the highway since it was constructed. The common types of landslides identified in the area were rock slumps, rock falls, wedge slides, toppling, soil slides and soil slumps. From the lithological standpoint, ten units described in Table 1 have been identified from the geological maps of the area. The study area is dominated by the three main rock types, namely sedimentary, igneous and metamorphic. Igneous and metamorphic rocks cover the middle and eastern part of the area while the sedimentary rocks are commonly found in the west.
Landslide influencing data layers
Geology: In the domain of landslide susceptibility mapping both the lithology
and structural geology play an important role. Lithology is a primary parameter
conditioning landslide occurrences as various lithological units have diverse
susceptibilities to landslides. Hence, a lot of researchers have utilized lithology
as an input factor to measure the vulnerability of landslides (Akgun
et al., 2008; Bai et al., 2010; Mezughi
et al., 2011). In this study, geological maps produced by Minerals
and Geoscience Department Malaysia at a scale of 1:63, 300 covering the study
area and the geologic formations were identified.
Table 1: 
Lithological units 


Fig. 1: 
Location of the study area shown with the TIN map 
The structural details such as strata dip and foliation dip, were acquired
from the above mentioned maps and from field studies. A total of 200 readings
representing strata dip and strike and 230 reading representing foliation dip
and strike were digitized as points and then they were interpolated to generate
strata and foliation dip maps.
Fractures are also considered as important geological structures which influence landslides. They can be detected from satellite images where they appear as linear to curvilinear features (lineaments). It has generally been observed that the probability of landslide occurrence increases near to lineaments which describe weakness zones. This study has used Landsat7 ETM+image to extract lineaments using various image processing and enhancement techniques. The interpreted lineaments were digitized in vector mode and converted to shape file to generate the lineament density map using the line density analyst extension on ArcGIS 9.2.
Topography: The Digital Elevation Model (DEM) represents the terrain
surface which is very important to generate many of topographic parameters which
control landslide activity in the area. The DEM was produced from a Triangulated
Irregular Network (TIN) model, acquired from contour lines and elevation points
on the 1:50,000 scale topographic maps with a contour interval of 20 m. Slope
angle, slope aspect and curvature are the significant topographic factors that
control landslide occurrence. They are automatically acquired from DEM and categorized
into different classes.
Slope: The slope angle is the primary factor is used in the slope stability
analysis (Lee and Min, 2001) and since it directly influences
landslides, it is often employed in generating landslide susceptibility maps
(Mancini et al., 2010; Kolat
et al., 2006). According, to Anbalagan (1992)
many previous studies indicate that the slope gradient is proportional with
the susceptibility of landslide occurrences. Hence, the slope factor plays a
vital role in generating landslide susceptibility maps. The relief of the study
area varies between 60 to 1200 m from mean sea level and therefore, it becomes
responsible for the major slope variation in the area that ranges from 0 to
88°.
Aspect: The slope aspect is another frequently used and stilldebated
instability factor as different conclusions are drawn by different authors in
different areas (Ercanoglu et al., 2004; Lee,
2005). The slope aspect contribute to landslide occurrence when the slope
face intense rainfall, sunlight and drying winds. It will ultimately affect
the other factors like the flora distribution, degree of water saturation, evapotranspiration
of the slope and the soil thickness. Climatic aspects like the intensity of
the rain and the amount of sunshine could influence landslides in that particular
slope, for instance the hillsides that receive dense rainfall are considered
to be more prone to landslides because, soils of these hillsides reach saturation
faster, causing the increase of pore water pressure. The saturation capacity
is also controlled by a few factors like the slope curvature, soil type, permeability,
porosity and land cover.
Curvature: Curvature represents the morphology of the topography which plays a significant role in the landslide phenomenon. It is considered as a factor that controls landslide occurrences due to its effect on the hydrological conditions of the soil cover. Generally, after rain fall, the soil in concave slope will retain and preserve more water than soils in convex slope. However, in a lot of places the convex slopes represent the outcrop of strong bedrock. Subsequently, the concave slope areas have a very high prospect for a landslide incidence than the convex areas. In the curvature raster file, the positive curvature values specify that the surface is convex at those cells. In contrast the negative principles designate that the surface is concave at those cells. A value of zero specifies that the surface is flat.
Topography/bedding relationship: The different geometric relationships
between bedding attitude and slope aspect can be considered as a factor that
controls landslide occurrence which is used in susceptibility mapping. Slope
stability can be influenced by geological structures as result of the angular
relationship between bedding attitude, slope aspect and slope angle (Wen
et al., 2004; Wu et al., 2004; Jaboyedoff
et al., 2004). In this study, dip angle and dip direction measurements
were taken from geological maps and from field surveys. The readings of the
dip direction and angle were interpolated using ordinary kriging to produce
dip angle and dip direction map, while the slope aspect and slope angle map
were calculated from DEM. Bedding direction and slope aspect datasets were overlaid
and according to their relationship four classes were identified as following:
Class 1: 
Layers dip opposite the slope 
Class 2: 
Layers dip as the slope and incline equal to the slope 
Class 3: 
Layers dip as the slope and incline more than the slope 
Class 4: 
Layers dip as the slope and incline less than the slope 
Classes 1, 2 and 3 represent the stable condition, while class 4 represents
the unstable condition because the bedding plane daylights on the slope's free
face.
Drainage: The proximity of the slopes to the stream networks is yet
another important factor that influences slope stability. Streams have a major
role in the slope stability by saturating the soil until the water level causes
the increase in the pore soil pressure and they can also heavily influence the
slope stability by toe erosion. According, to Cevik and
Topal (2003) the higher stream density the lower is the penetration of water
into soil and the faster is the movement of surface flow. Generally, the penetration
happens on slopes adjacent to the streams, which have a high permeability such
as alluvium. In order to produce drainage density map in this study, the drainage
were digitized from topographic maps of scale 1:50.000 and a drainage density
map was calculated using the line density analyst extension on ArcGIS 9.2. The
drainage density map was classified into five equal intervals classes.
Rain fall: Among the natural activities the rainfall is the primary catalyst that induces the landslides. Rainfall is the main triggering factor for Landslides in the area where most of the landslides occurred after heavy rainfall. A rainfall map was generated by this study based on annual rainfall data collected from three meteorological stations for the period of 2000, 2005 and 2009. The rainfall map was generated using interpolation method. Based on the analysis the maximum rain fall recorded in the eastern part of the area is 3970 mm year^{1} and the lowest rainfall is recorded in the western part is 1590 mm year^{1}.
Distance from road: Roads are considered as one of the important anthropogenic
factors controlling slope stability. Landslides might happen on the road and
on slopes of road sides (Pachauri et al., 1998).
It has been observed that, many landslides occur close to roads. The reason
for this is the extraction of materials from the lower portion of the slopes
during road construction, which eventually makes the slope lose to support and
also due to the frequent vibrations generated by vehicles predispose hill slopes
to failure. During the field visits of this study, most landslides were detected
due to road construction work. In this study the road distance map was generated
by digitizing the road network from the topographic maps and the area was classified
into five distance buffer classes, computed at 100 m intervals from both sides
of the roads to determine the effect of the road on the stability of slope.
Soil: Soil is another significant factor that is employed to evaluate the occurrence of landslides. The topsoil cover on a slope has an influence on landslide occurrence as observed in the field. For this study, a soil map was prepared using 32 soil samples collected in the field from residual soils formed by weathering processes on the rocks. The soil samples were classified in the laboratory based on the Unified Soil Classification System (USCS). The study has identified the following types of soil: SILTsandy and SANDsilty.
AHP method: The Analytic Hierarchy Process (AHP) is a structural framework
that enhances the realization of complicated decisions by decomposing the issue
in a hierarchical structure. This approach breaks down a composite, amorphous
circumstance into its components parts, organizing these parts or judgments
on the relative significance of every variable and synthesizing the judgments
to establish the variables that have the maximum priority and must be acted
upon to influence the resulting situation (Saaty, 1990).
The AHP is a subjective approach that is employed in landslide susceptibility
evaluation depending on understanding and knowledge of the experts to decide
the factors affecting the landslide process. It is utilized to ascertain the
relative importance of all the criteria (factors) and sub criteria (classes)
that contribute to landslide susceptibility to compute its weight. This is implemented
by constructing a hierarchy of decision criterions (causative factors) that
are compared to each other in pairwise assessment in a matrix in which every
factor is rated with other factors by giving a score value. The scores are provided
based on the comparative precedence of the factor for influencing landslides
and depending on the estimation of an expert following the rating system (Table
2) introduced by Saaty (1977). The ranking of the
relative priority of the criteria is performed by allotting a weight between
1 that signifies equal importance and 9 that indicates extreme importance to
the more vital criterion, whereas, the reciprocal of this value is assigned
to the other factor in the pair. When the factor on the vertical axis of the
matrix is more significant than the feature on the horizontal axis, the value
differs between 1 and 9. On the other hand, the value differs between the reciprocals
between 1/2 and 1/9. To compute an average weight for each factor, the columns
are initially normalized by dividing the elements of every column by the sum
of the column and then summing all the elements in each resultant row and divide
this sum by the number of elements in the row. The summary of the outcome for
this computation are illustrated in Table 3.
As the comparisons are accomplished by personal or subjective judgments, some
degree of inconsistency may occur, hence, Consistency Ratio (CR) which is an
index of inconsistency, is employed to specify that the matrix judgments were
randomly generated (Saaty, 1980). The CR is acquired as
follows:
where, CI is the consistency index which is expressed as:
where, λ_{max} is the major or principal eigenvalue of the matrix and it is computed from the matrix and n is the order of the matrix.
The Random Consistency Index (RI) is the average of the consequently constancy
index based on the order of the matrix proposed by Saaty (1980).
Table 2 illustrates the value of the Random Consistency Index
(RI) for matrices of order 1 to 10 acquired by approximating random indices
using a sample size of 500 (Saaty, 2000).
The acceptable CR range varies based on the size of matrix i.e., 0.05 for a
3 by 3 matrix, 0.08 for a 4 by 4 matrix and 0.1 for all larger matrices, n≥5
(Saaty, 2000; Cheng and Li, 2001).
Thus, a CR of 0.1 or less is a practical level of reliability (Malczewski,
1999) whereas, a CR above 0.1 needs revision the judgment in the matrix
due to conflicting treatment of particular factor ratings.
RESULTS AND DISCUSSION
After the application of the AHP, the acquired weight values of causative factors
(W_{i}) and the ranking values (R_{i}) of the different classes
in these factor layers were acquired from the Eigenvalues of the AHP matrixes
that articulates the relation between various factors and of the matrixes that
represent the relationship between classes in a factor.
Table 2: 
Scale of relative importance suggested by Saaty
(1977) 

The consistency of the weights and ratings are validated by taking the principal
eigenvectors of each matrix and computing the consistency index CI and consistency
ratio CR. In all cases of the gained class weights with CR_{s}<0.1,
the ratio illustrates a sensible level of consistency in the pairwise comparison
that was adequate to identify the class weights. In this study, the CR ranges
between 0.00 and .0987, signifying a rational level of consistency in the pairwise
comparison, that is reasonable to identify the factor weights. After computing
the weight of each factor and the rate of each class using AHP method, the Landslide
Susceptibility Index (LSI) was calculated by summing up each factor’s weight
multiplied by class weight of every referred factor (for that pixel) written
as follows:
where, LSI is the calculated landslide susceptibility index of the given pixel, R_{i} and W_{i} are class rating value and the factor weight for factor i which is derived using AHP technique (Table 3). The LSI values characterize the comparative susceptibility of a landslide occurrence, hence, if the index is higher the area will be more prone to landslides.
To verify the results, the LSI was compared with known landslides. The LSI was assessed in terms of its predictive power validity by calculating the prediction rate curve. To produce the prediction rate curve, the computed index values of all cells in the targeted area were arranged in descending order and divided into 100 equal classes ranging from very highly susceptible classes to non susceptible classes. Then, the 100 classes were overlaid and intersected with known landslides to establish the percentage of landslide incidences in each susceptible class. Figure 2 illustrates the prediction rate curve as a line graph. The Fig. 2 also indicates the satisfactory results, highest susceptibility pixels that envelop 10% of the study area includes 56% of known landslides, while the 20% high susceptible area covers more than 68% of landslides. Later, the prediction of the map was validated more precisely using the Area Under the Curve (AUC) by ascertaining that the ideal prediction will have highest AUC of 1. In our study, the AUC was found to be 0.8097.
Table 3: 
Pairwise comparison matrix with classes ratings (R_{i})
and factor weights (W_{i}) 

Consequently, it indicates that the prediction precision of the acquired map is 80.97% with respect to the ideal value of 100%, which is comparatively satisfied.
Finally, all the identified values of LSI were categorized into five classes by employing the natural breaks algorithm to signify five classes of the Landslide Susceptibility Zone (LSZ) of the area; namely, i) very high, ii) high, iii) moderate, iv) low and v) very low susceptibility zones (Fig. 3). The five susceptibility zones were overlaid and crossed with the landslide location map. Figure 4 shows a histogram that abridges the outcome of the complete process.

Fig. 2: 
Cumulative frequency diagram showing percentage of study area
classified as susceptible (xaxis) in cumulative percent of landslide occurrence
(yaxis) 

Fig. 3: 
Landslide susceptibility map of the study area 

Fig. 4: 
The percentage distribution of the susceptibility classes
and landslide occurrence 
CONCLUSION
This study has provided a landslide susceptibility assessment model with the aid of GIS for a landslide prone area located in central northern Malaysia. This model is cost effective and capable of quickly contributing to the landslide assessment by manipulating data and performing the essential analysis. In order to accomplish this purpose ten landslide control factors were employed in the analysis which includes: slope gradient, slope aspect, curvature, distance from road, drainage density, lithology, foliation dip, topographic/bedding relationship, lineament density, soil and rainfall. An Analytical Hierarchical Process was implemented in order to obtain the weights for every factor and class using direct pairwise comparison, later based on these weights, thematic maps of factors were combined by weighted overly techniques and the landslide susceptibility map of the study area was created.
The obtained map was classified into five susceptibility classes which specified that the high and very high susceptible zones include about 24.3% of the total area, while about 45.2% were classified as low and very low susceptible zones and 30.4% is moderately susceptible zone. At the end, the map was validated with known landslides data based on the Area Under Curve (AUC) method, by which the prediction precision of 80.97% was established.