U.S. Department of the Interior

U.S. Geological Survey

Pamphlet to accompany

Scientific Investigations Map 3353

Map of Landslides Triggered by the January 12, 2010, 

Haiti Earthquake
Cover. Landslides triggered by the 2010 Haiti earthquake. Photograph by R.W. Jibson, March 2010.
Map of Landslides Triggered by the 

January 12, 2010, Haiti Earthquake

By Edwin L. Harp, Randall W. Jibson, and Robert G. Schmitt

Pamphlet to accompany

Scientific Investigations Map 3353

U.S. Department of the Interior

U.S. Geological Survey
U.S. Department of the Interior

SALLY JEWELL, Secretary

U.S. Geological Survey

Suzette M. Kimball, Director

U.S. Geological Survey, Reston, Virginia: 2016

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Suggested citation:

Harp, E.L., Jibson, R.W., and Schmitt, R.G., 2016, Map of landslides triggered by the January 12, 2010, 

Haiti earthquake: U.S. Geological Survey Scientific Investigations Map 3353, 15 p., 1 sheet, scale 1:150,000, 

http://dx.doi.org/10.3133/sim3353.

ISSN 2329-132X (online)
iii

Contents

Abstract...........................................................................................................................................................1

Introduction.....................................................................................................................................................1

Description of Study Area ............................................................................................................................1

The 2010 Haiti Earthquake............................................................................................................................3

Mapping and Interpretation.........................................................................................................................3

Landslides Triggered by the Earthquake....................................................................................................3

Landslide Types.....................................................................................................................................3

Numbers and Distribution ...................................................................................................................4

Geologic Units Involved in Landslides ..............................................................................................4

Topography ............................................................................................................................................4

Seismic Shaking....................................................................................................................................4

Discussion.....................................................................................................................................................13

Summary and Conclusions.........................................................................................................................13

References Cited..........................................................................................................................................13

Sheet

1. Landslides triggered by the January 12, 2010, Haiti earthquake..................................... link

Figures

1. Geologic map of landslide-affected area.................................................................................2

2. Map of landslide concentration (percent/km2) in the landslide-affected area..................5

3. Rock fall composed of lower Miocene limestone boulders that have failed along

preexisting fractures....................................................................................................................6

4. Shallow soil slides in weathered volcanic regolith within the Enriquillo–Plantain

Garden fault zone..........................................................................................................................6

5. Histograms of triggered landslides with respect to geology and slope..............................8

6. Detail of fault-slip model of Hayes and others (2010) on map showing landslides

and geology .................................................................................................................................10

7. Detail of fault-slip model of Symithe and others (2013) on map showing landslides

and geology .................................................................................................................................11

8. Map of landslide densities overlain by ShakeMap contours of PGA (peak ground

acceleration) from the earthquake..........................................................................................12

Tables

1. Areal distribution of earthquake-triggered landslides within geologic units.....................7

2. Areal distribution of earthquake-triggered landslide for different rock types...................9
iv

Conversion Factors

International System of Units to Inch/Pound

Multiply By To obtain

Length

meter (m) 3.281 foot (ft) 

kilometer (km) 0.6214 mile (mi)

Area

square kilometer (km2

) 0.3861 square mile (mi2)

Volume

cubic meter (m3

) 1.308 cubic yard (yd3)

Datum

Coordinate information is referenced to the World Geodetic System 1984 (WGS 84).

Abbreviations

ASTER Advanced Spaceborne Thermal Emission and Reflection Radiometer

DEM digital elevation model

DYFI “Did You Feel It?”

EPGFZ Enriquillo–Plantain Garden fault zone

g acceleration of gravity (9.8 meter per second squared; m/s2)

GPS global positioning system

GSN Global Seismic Network

InSAR Interferometric Synthetic Aperture Radar

M magnitude (earthquake)

MMI modified Mercalli intensity

NOAA National Oceanic and Atmospheric Administration

PGA peak ground acceleration

USGS U.S. Geological Survey
Map of Landslides Triggered by the January 12, 2010, 

Haiti Earthquake

By Edwin L. Harp, Randall W. Jibson, and Robert G. Schmitt

Abstract

The magnitude (M) 7.0 Haiti earthquake of January 12, 

2010, triggered landslides throughout much of Haiti on the 

island of Hispaniola in the Caribbean Sea. The epicenter of 

the quake was located at 18.44°N., 72.57°W. at a depth of 

13 kilometers (km) approximately 25 km southwest of the 

capital, Port-au-Prince. Although estimates vary widely, the 

most reliable surveys of casualties indicate that the earthquake 

caused 158,679 fatalities and more than 300,000 injuries. The 

U.S. Geological Survey compared publicly available satellite 

imagery acquired both before and after the earthquake and 

mapped 23,567 landslides that were triggered by the strong 

shaking. Our mapping from aerial photography and satellite 

imagery was augmented by field observations.

Most of the landslides triggered by the earthquake were 

south of the Léogâne fault on the footwall and were fairly 

shallow falls and slides in weathered limestone (2–5 meters 

[m] thick) and volcanic rock and soil (generally <1 m thick). 

Landslides extended from the north to the south coasts of 

the southwestern peninsula (southwest of Port-au-Prince) 

and almost 60 km to the east and west of the epicenter. The 

highest concentration of landslides was on the steep limestone 

slopes of incised river valleys, but large numbers of landslides also occurred on gentler slopes in weathered volcanic 

rocks. Although some high landslide concentrations did occur 

near areas of maximum fault slip, the overall distribution of 

landslides appears to involve complex interactions between 

geology, topography, and strong shaking with limited spatial 

correlation between fault slip and landslides.

Introduction

The January 12, 2010, Haiti earthquake (magnitude 

[M] 7.0) caused widespread damage and casualties. Haiti is 

located on the western one-third of the island of Hispaniola 

in the Caribbean Sea. One of the most prevalent effects of 

this earthquake was the triggering of tens of thousands of 

landslides from steep slopes throughout much of the country. 

Documenting the distribution and concentration of these landslides is important to understand the geologic, seismologic, 

and topographic factors that control this distribution; such 

information is important for assessing future landslide hazards in both Haiti and elsewhere.

Using a combination of pre- and post-earthquake satellite 

imagery and aerial photography, we mapped 23,567 landslides triggered by the earthquake within an area of about 

5,000 square kilometers (km2

) (see map sheet). Most of the 

landslides triggered by the earthquake were south (on the 

footwall) of the seismogenic Léogâne fault, a blind thrust fault 

not exposed at the ground surface. Two other inventories of 

landslides triggered by this earthquake have been produced: 

Gorum and others (2013) mapped 4,490 landslides, and Xu 

and others (2014) mapped 30,828 landslides. Both of these 

inventories were produced solely by interpretation of imagery, 

whereas our mapping from aerial photography and satellite 

imagery was augmented by our field investigation in March 

2010. Differences in numbers of landslides in these inventories probably stem from differences in (1) the extent of the 

areas examined, (2) the quality and resolution of remotely 

sensed imagery used, (3) how coalescing landslides from 

multiple sources are counted, and (4) subjective interpretation 

of features visible in the imagery.

In this report, we present a map and a data file of triggered landslides (as polygons); we briefly describe the 2010 

earthquake and describe the landslide distribution with respect 

to geology, topography, and strong shaking.

Description of Study Area

Haiti occupies the western one-third of the island of 

Hispaniola. Haiti’s terrain consists primarily of rugged mountains interspersed with narrow river valleys and small coastal 

plains. Elevations range from sea level up to 2,680 meters (m). 

The climate is tropical, with average annual rainfall of about 

1,440 millimeters (mm) (http://mecometer.com/whats/haiti/

average-yearly-precipitation/).

A geologic map of the study area (fig. 1) shows that the 

central mountainous core of the southern peninsula consists of Cretaceous andesitic and basaltic basement rock and 

Cretaceous-Tertiary limestone and clastic sedimentary rock. 

Quaternary deposits include alluvium deposited in the PortAu-Prince valley and interior incised river valleys, alluvial 
Figure 1. Geologic map of landslide-affected area. Colors are used to group units broadly by lithology and age. Volcanic rocks (red); calcareous (tan). From Bureau des Mines et de l’Energie (2005).

73°00' 72°75' 72°50' 72°25' 

18°50'

18°25'

18°00'

Cb

Cb

Cb

Cb

Qac

Qa

Qa

Cc

Cs

Cs

Ems Ep

Mi

Mm

Pi

Cb

Cb Cb Ems Cc

Ems

P

P

Qa

O

Cb

Ems

Ep Ep

Mi

Mi

Mm

Mm

O

Cb Cb

Cb

Cb

Cs

Cs

Cs Ems

Ems

Ems

Ems Ems

Ems

Ems

Ems

Ep Ep Ep

Mm

Pi

Qa

Qa

Qa

Qc

O

Ca

Cb

Cb

Cs

Cs

Cs

Cs

Cs

Ems

Ep

Ep

Ep

Ep

Mi

Pi

Pi Qa

Qa

Qc

Qc

O

Cs

Cs Ems

Ems Ep

Ep

Mi

P

Cs

Cs

Ems

Ep

Mi

Mi Mi

P

Pi

Qa

O

O

Mi

Ms

P

Qac

Qac

Cb

Cb

Cb

CbCb

Ep

Ep

Ms

Ep

Qa

Qa

Qa

Qa

Es M

Ms

P

Qa

Qac 

E

Ems

Ems

Ems

Qa

Grand-Goâve

Petit-Goâve

Bainet

Jacmel

Port-au-Prince

Bainet

Rivière

Rivière

Rivière

Rivière

Grande

Gauche

Rivière Grosseline

Rivière Froide

de Jacmel

Momance

Base map data from a variety of sources (see pamphlet), accessed from http://hdds.usgs.gov/ between January 2013 and January 2014Projection: Universal Transverse Mercator, zone 18; World Geodetic System 1984 (WGS 84); False easting 500000.0, false northing 0.0, central meridian –75.0

Baie de

Port-au-Prince

Canal du Sud

CARIBBEAN SEA

ENRIQUILLO-PLANTAIN GARDEN FAULT ZONE

Quaternary Tertiary 

EXPLANATION

Landslides triggered by earthquakes

Major rivers

Roads

Epicenter

Alluvium

Alluvium and reef limestone

Reef limestone

Upper Pliocene to middle and lower Eoc

Conglomerate and volcanic sandstonsandstone, limestone and marl; limest

Middle to upper Eocene—Pelagic biomiOligocene—Chalk and limestone marl; c and sandstone; limestone and conglom

Upper Eocene—Pelagic limestone

Lower Miocene—Sand-clay flysch;

calcareous sandstone; limestone

Middle Miocene—Blue-gray marl;

pelagic limestone

Upper Miocene—Marl and sand

Pliocene—Marl and sand

Note: Colors may appear slightly different on the map because of the applicat

Qa

Qc

Qac 

P

Ms

Mm

Mi

Es

O

Ems

Ep

Base from esri, accessed on Dec. 3, 2015 athttp://www.arcgis.com/home/webmap/viewer.html

0 5 10 15 20 KILOMETERS0 5 10 15 20 MILES

HAITI

DOMINICAN

REPUBLIC

CUBA

FIGURE

AREA
Landslides Triggered by the Earthquake 3

fan and colluvial wedge deposits along the margins of larger 

valleys, and coastal delta fan complexes where larger rivers 

discharge into the sea along the coast.

The 2010 earthquake occurred near the EnriquilloPlaintain Garden fault zone (EPGFZ), a major left-lateral fault 

zone that defines part of the boundary between the Caribbean and North American tectonic plates. The plate boundary 

accommodates an average of 20 millimeters per year (mm/yr) 

of left-lateral displacement between the plates (U.S. Geological Survey, 2010a). The fault extends east-west along the 

north part of the southern Haiti peninsula and has exerted a 

substantial geomorphic influence on the region. Continuing 

strike-slip fault displacement has formed linear valleys and 

bounding uplifted mountains, shutter ridges, and sag ponds 

along the fault trace. Some river valleys, most strikingly the 

deep valley of the Rivière Momance, follow the EPGFZ trace 

and are apparently the result of preferred incision of sheared 

and locally weaker rocks along the fault zone. 

The 2010 Haiti Earthquake

On January 12, 2010, an M7.0 earthquake struck approximately 25 km southwest of the capital of Haiti, Port-au-Prince, 

at 16:53 local time. The epicenter of the quake was located 

at 18.44°N., 72.57°W. at a depth of 13 km (U.S. Geological 

Survey, 2010a). Although estimates vary widely, the most reliable surveys of casualties indicate that the earthquake caused 

158,679 fatalities (Kolbe and others, 2010) and more than 

300,000 injuries (Cavallo and others, 2010). The earthquake 

was initially attributed to displacement within the left-lateral 

EPGFZ. However, joint inversion of Interferometric Sythetic Aperature Radar (InSAR) data, coastal uplift/subsidence 

from global positioning system (GPS) data, and teleseismic 

body waves (Calais and others, 2010; Hayes and others, 

2010; Symithe and others, 2013) indicated that the preferred 

model of fault slip involves complex movement on as many 

as three faults, with about 80 percent of the moment released 

from movement on a 55° north-dipping blind thrust called 

the Léogâne fault (Hayes and others, 2010) located just to the 

north of the EGPFZ. 

No strong-motion records are available from the earthquake. The U.S. Geological Survey (2010b) ShakeMap model, 

described in detail subsequently, estimated that peak ground 

accelerations (PGA) exceeded 0.9 acceleration of gravity (g) 

near the epicenter (Worden and others, 2010).

Mapping and Interpretation

We acquired imagery after the earthquake from a variety 

of sources (all of the imagery was accessed through the U.S. 

Geological Survey [USGS] at http://hdds.usgs.gov/) including the following: Google Earth; Digital Globe’s Quickbird, 

Geoeye, and Worldview 2; National Oceanographic and 

Atmospheric Administration (NOAA) aerial photography; 

and Microsoft Ultracam G aerial photography. All of this 

imagery has a resolution of less than 1 m. Google Earth 

posted many different sources of imagery including their 

own. The highest resolution and best true color was from 

Google Earth’s aerial photography taken on January 24, 2010. 

Its resolution is about 0.3 m, but its coverage is limited. We 

eventually settled on using the Microsoft Ultracam G aerial 

photographs taken on January 28, 2010, because of its high 

resolution (approximately 0.6 m), complete coverage of the 

country, near-vertical view, and advantage of being largely 

free of clouds. This imagery allowed us to thoroughly map 

all landslides triggered by the earthquake and achieve mapping consistency throughout the study area. Where possible, 

we compared pre- and post-earthquake imagery to confirm 

our interpretations of coseismic triggering. In some places, 

especially in the southeastern part of the study area, preearthquake imagery was not available. In March 2010, we 

carried out helicopter reconnaissance of the landslide-affected 

area in Haiti and conducted ground surveys of significant 

landslides (Jibson and Harp, 2011). 

The imagery used was imported into esri’s ArcMap10.1 

and ArcGlobe 10.1. We identified the landslides and mapped 

them as polygons by digitizing them in ArcMap; the polygons were then transferred into ArcGlobe, where the imagery was draped onto a 30-m digital elevation model (DEM; 

ASTER Global DEM, resolution 1 arc-second for scene: 

ASTGDEMV2_0N18W073, accessed October 2011, and available at https://lpdaac.usgs.gov/dataset_discovery/aster/aster_

products_table/astgtm). The polygons could then be viewed 

in a pseudo-three-dimensional perspective, which aided in the 

identification of landslides and the interpretations of the topography of surrounding slopes. The earthquake-triggered landslides generally appeared lighter in color than the surrounding 

slopes (especially within the limestone terrain); landslides commonly displayed fresh-looking cracks at the main scarps in the 

source areas and abundant fine particles and even dust at many 

of the distal areas beyond the landslide toes. Each polygon 

includes all of the landslide features (source, travel path, and 

deposit); no attempt was made to separate these features.

Landslides Triggered by the Earthquake

Landslide Types

The most common types of landslides triggered by the 

earthquake were shallow, disrupted rock falls and rock slides 

(landslide terminology after Varnes, 1978; and Keefer, 1984) 

in limestone and highly weathered volcanic rocks, primarily 

basalt and andesite (Harp and others, 2013). In addition to 

shallow rock falls and rock slides, the earthquake triggered 

less numerous, deeper rotational slumps, rock-block slides, 

and earth flows, some of which blocked drainages and formed 

small, temporary lakes after the earthquake. Most of the 

deeper landslides occurred in slopes underlain by limestone; 
4 Map of Landslides Triggered by the January 12, 2010, Haiti Earthquake

however, a few occurred in weathered volcanic rocks. The 

largest of these deeper landslides was located about 20 km 

south of Petit-Goâve and had a volume of about 2,400,000 

cubic meters (m3).

Numbers and Distribution

Our inventory includes 23,567 triggered landslides (see 

map sheet). Landslides extended from the north coast to the 

south coast of the southwestern peninsula, where the epicenter 

was located. Landslide epicentral-distance limits were symmetrical about the epicenter to the southwest and the southeast at 58 km. Figure 2 shows the spatial distribution of local 

landslide concentration (percentage area covered by landslides 

within each square kilometer). Two areas of highest local 

landslide concentration are apparent: one about 10 km east 

of the epicenter along the Rivière Momance within and south 

of the EPGFZ, and another about 20 km west-southwest of 

the epicenter south of Grand-Goâve. Both of these areas have 

local landslide concentrations exceeding 20 percent; the area 

along the Rivière Momance near the EPGFZ had the highest 

concentration at greater than 40 percent. These areas of highest local landslide concentration occurred along major river 

drainages where the steepest slopes are present.

Geologic Units Involved in Landslides

The predominant rock types in which landslides occurred 

in the area south of Port-au-Prince are Tertiary calcareous 

rocks (predominantly limestone) and Cretaceous weathered 

volcanic rocks (fig. 1). Cretaceous limestone also intermingles 

with Cretaceous volcanic rocks in the region surrounding 

the northwest-southeast oriented valleys of the Gauche and 

Grand-Goâve Rivers that extend from Jacmel on the southeast to Grand-Goâve on the northwest (fig. 1). The limestone 

ranges from moderately weathered hard rock to more deeply 

weathered and hydrothermally altered rock that is fractured 

and blocky (fig. 3). Rock falls and rock slides in these calcareous rocks failed along preexisting fractures and consist 

of cobble- to boulder-sized fragments. Thicknesses of falls 

and slides in the limestone typically ranged from 2 to 10 m. 

Failures within the weathered volcanic rock generally were 

much thinner and occurred within the weathered regolith or 

colluvium; such failures ranged from 0.2 m to several meters 

in thickness (fig. 4). 

Table 1 lists the geologic units, the area covered by 

landslides within each unit, the total area of each unit within 

the map area, and the percentage of each unit covered by 

landslides; this information is shown graphically in figure 5. 

Figure 5A shows that the two units having the highest numbers 

of landslides were the calcareous unit Ems (8,917 landslides) 

and the basaltic unit Cb (5,861 landslides). Although unit 

Ems had the greatest number of landslides and the highest 

local landslide concentration (42 percent in areas of abundant 

steep slopes), table 1 and figure 5B show that the highest 

overall landslide concentration by far occurred in the Cretaceous limestone unit Cs (2.549 percent). This unit crops 

out at the western end of the fault-rupture zone and contains a dense concentration of landslides (see fig. 2 and map 

sheet). All other units had landslide concentrations less than 

1 percent. Among calcareous units, Mi (0.885 percent), Ems

(0.657 percent), Ep (0.647 percent), and O (0.639 percent) 

form the next tier of landslide concentrations. The two volcanic units had concentrations similar to these calcareous units: 

Ca (0.648 percent) and Cb (0.619 percent). These concentrations are broadly consistent with the findings of Xu and others 

(2014), who list landslide area percentages for their three highest concentrations as Cs (1.75 percent), Mi (0.84 percent), and 

Ca (0.72 percent). The overall landslide concentration in the 

study area was 0.564 percent.

Landslide numbers, areas, and concentrations with the 

geologic units are generalized into three rock types: alluvium, 

calcareous rocks, and volcanic rocks (table 2). Calcareous 

units accounted for 70 percent of the total number of landslides and 77 percent of the overall landslide area (table 2). 

Volcanic units accounted for 28 percent of the landslides and 

23 percent of the landslide area. Landslides in alluvium were 

a negligible fraction of the landslides and landslide area. 

Because calcareous rocks are far more extensive than volcanic 

rocks, however, landslide concentrations in these rock types 

were nearly identical (0.631 and 0.621 percent, respectively). 

Topography

The topography in Haiti on the peninsula south of Portau-Prince is characterized by upland plateaus dissected by 

steep canyons. Most of the landslides triggered by the earthquake occurred within or along these canyons. The distribution 

of slopes on which landslides occurred (fig. 5C) shows that the 

maximum number were on slopes of about 35°.

Although some landslides from this earthquake originated 

near the crests of ridges, most occurred within the steep inner 

gorges along rivers at some distance below the ridge crests. 

This contrasts with observations from some other worldwide 

earthquakes where triggered landslides were concentrated 

most heavily along ridge crests (Meunier and others, 2008). 

In many of the river drainages in Haiti, the steepest slopes are 

concentrated near the river channel. 

Seismic Shaking

At the time of this earthquake, there were no seismic 

instruments in Haiti. The closest seismic instrument was located 

in the Dominican Republic within the abutment of a dam. The 

Dominican Republic occupies the eastern two-thirds of the 

island of Hispaniola. Using teleseismic body-wave data, coastal 

uplift/subsidence data from GPS measurements, and InSAR 

data, multiple models of the fault source and its slip have been 

constructed (Calais and others, 2010; Hayes and others, 2010; 

Symithe and others, 2013). These models show variations in 
Figure 2. Map of landslide concentration (percent/km2) in the landslide-affected area.

EXPLA

Landslides triggere by earthquakes

Major rivers

Roads

Epicenter 

73°00' 72°75' 72°50' 72°25'

18°50'

18°25'

18°00'

Rivière Momance

Grand-Goâve

Petit-Goâve

Bainet

Jacmel

Port-au-Prince

Bainet Rivière

Rivière

Rivière Grande

Gauche Rivière Grosseline

Rivière Froide

de Jacmel

Base map data from a variety of sources (see pamphlet), accessed from http://hdds.usgs.gov/ between January 2013 and January 2014Projection: Universal Transverse Mercator, zone 18; World Geodetic System 1984 (WGS 84); False easting 500000.0, false northing 0.0, central meridian –75.0

Baie de

Port-au-Prince

CARIBBEAN SEA

Canal du Sud

ENRIQUILLO-PLANTAIN GARDEN FAULT ZONE

0 5 10 15 20 KILOMETERS0 5 10 15 20 MILES

FIGURE

AREA

Base from esri, accessed on Dec. 3, 2015 athttp://www.arcgis.com/home/webmap/viewer.html

HAITI

DOMINICAN

REPUBLIC

CUBA
6 Map of Landslides Triggered by the January 12, 2010, Haiti Earthquake

Figure 3. Rock fall composed of lower Miocene limestone boulders that have failed along preexisting 

fractures. Photograph taken along the Rivière Momance about 20 km west-southwest of Port-Au-Prince (see 

fig. 1). Photograph by R.W. Jibson, March 2010.

Figure 4. Shallow soil slides in weathered volcanic regolith within the Enriquillo–Plantain Garden fault zone. 

Landsides are visible as lighter colored, unvegetated areas. Photograph taken about 20 km southwest of PortAu-Prince (see fig. 2). Photograph by E.L. Harp, March 2010.
Landslides Triggered by the Earthquake 7

Table 1. Areal distribution of earthquake-triggered landslides within geologic units in the study area.

[Square kilometers, km2; Geologic units from Bureau des Mines et de l’Energie (2005)]

Geologic unit1 Rock type Number of landslides Area of landslides 

(km2

)

Area of geologic unit 

within study area 

(km2

)

Percentage of unit 

covered by

landslides

Qa Alluvium 347 0.16 475.80 0.034

Qc Calcareous 265 0.17 83.51 0.199

Qac Calcareous 20 0.01 193.06 0.004

P Calcareous 351 0.20 190.72 0.106

Ms Calcareous 362 0.36 92.56 0.386

Mm Calcareous 118 0.08 174.24 0.049

Mi Calcareous 1,945 1.50 169.24 0.885

Es Calcareous 25 0.06 29.03 0.214

O Calcareous 683 0.73 114.12 0.639

Ems Calcareous 8,917 9.87 1,502.58 0.657

Ep Calcareous 1,741 1.65 254.12 0.647

Pi Calcareous 116 0.15 31.67 0.480

Cs Calcareous 2,038 4.19 164.49 2.549

Cc Calcareous 4 0.01 6.04 0.116

Ca Volcanic 774 0.47 72.44 0.648

Cb Volcanic 5,861 5.09 822.16 0.619

Total 23,567 24.69 4,375.78 20.564

1

Units described in figure 1.

2

The total percentage of unit covered by landslides is the total landslide area divided by the total study area.
8 Map of Landslides Triggered by the January 12, 2010, Haiti Earthquake

Figure 5. Histograms of triggered landslides with respect to geology and slope: A, Numbers 

of landslides within each geologic unit (refer to fig. 1); B, Landslide concentration within each 

geologic unit (geologic units defined in fig. 1); C, Number of landslides within 5° slope ranges.

0.70

0.60

0.50

0.40

0.30

0.20

0.10

0.00

Ca Cb Cc Cs Ems Ep Es Mi Mm Ms P Pi Qa Qac Qc O

B

1,800

1,600

1,400

1,200

1,000

800

600

400

200 177

453

738

1,050

1,470 1,413

806

108

47 13 4 2 1

0–5 5–10 10–15 15–20 20–25 25–30 30–35 35–40 45–50 50–55 55–60 60–65 65–70 70–75 75–80 80–85

0

C

Geologic unit

Slope, in degrees

1,347

351

1,539

10,000

9,000

8,000

7,000

6,000

5,000

4,000

3,000

2,000

1,000

0

Ca Cb Cc Cs Ems Ep Es Mi Mm Ms P Pi Qa Qac Qc O

A

Geologic unit

Number of landslides Number of landslides Landslide concentration , in percent
Landslides Triggered by the Earthquake 9

the coseismic slip of the fault that could have influenced the 

spatial distribution of the landslides triggered by the earthquake. The model constructed by Hayes and others (2010) for 

the Léogâne fault plane, upon which 80 percent of the moment 

release occurred (fig. 6), indicates that the maximum fault slip 

occurred at the eastern edge of the fault source, approximately 

12 km from the area of the highest local landslide concentration 

along the Rivière Momance near and just south of the EPGFZ. 

Local landslide concentration immediately above the area of 

maximum fault slip was not high because the topography in that 

area is fairly flat. The other area of high landslide concentration 

south of Grand-Goâve is 8 km south-southwest of the westernmost slip maxima (fig. 6). The slip vectors in the fault-slip 

model (fig. 6) point in a south to south-southwest direction in 

the vicinity of the region of maximum slip near the eastern edge 

of the fault-source model; slip vectors near the westernmost slip 

maxima point west-southwest. The distances from the area of 

maximum fault slip to the farthest landslides are 42 km to the 

southeast and 62 km to the southwest. 

Most of the earthquake-triggered landslides lie south of 

the fault source and epicenter, on the footwall of the Léogâne 

fault, in the general direction of thrust movement on the fault. 

This contrasts with other worldwide thrust earthquakes where 

the greatest numbers of landslides and the strongest ground 

motions were concentrated on the hanging wall (Abrahamson 

and Somerville, 1996; Harp and Jibson, 1996; Allen and others, 1998; Shabestari and Yamazaki, 2003; Chang and others, 

2004). However, the landslide distribution for this earthquake is 

strongly constrained by the distribution of steep topography—

the area north of the Léogâne fault, on the hanging wall, 

consists primarily of a fairly flat coastal plain truncated by the 

coastline with relatively sparse steep slopes. Thus, the relative 

lack of susceptible topography on the hanging wall constrains 

the landslide distribution mostly to the footwall. Other faultslip models (Symithe and others, 2013) are similar to that of 

Hayes and others (2010) except that they consist of two adjacent 

segments located slightly south of the fault source of Hayes 

and others (2010). The slip vectors (see fig. 7, modified from 

Symithe and others, 2013) are similar in magnitude and direction in the eastern segment to those in the model by Hayes and 

others (2010); in the western segment, however, the vectors 

trend more southerly than do those in the model of Hayes and 

others (2010) (fig. 6). The model in figure 7 is one of three 

constructed by Symithe and others (2013) for different weights 

of GPS, InSAR, and uplift data. In the other two models of 

Symithe and others (2013), the slip vectors in the western segment trend nearly west. Although the high local concentration 

of landslides in the Rivière Momance area is close (10–12 km) 

to the areas of maximum slip shown on both models, neither 

the Hayes and others (2010) nor the Symithe and others (2013) 

model have vectors that point directly toward this high landslide 

concentration. However, the Symithe and others (2013) version 

that we show in figure 7 does show slip vectors in the western 

segment that point directly toward the high local concentration of landslides south of Petit-Goâve, whereas the Hayes 

and others (2010) model shows vectors in the western portion 

of the model pointing more westward. In view of the south to 

southwest directivity of the coseismic slip on the Léogâne fault, 

especially that shown in figure 7, it is possible that the distribution of the majority of landslides to the south of the thrust fault 

in this area is in part a response to this directivity.

The lack of strong-motion instruments in the country 

at the time of the earthquake resulted in no local instrumental control on the pattern of ground shaking. Input into the 

local ground-shaking patterns displayed in ShakeMap are 

from the normal parameters used by ShakeMap (Worden and 

others, 2010) such as broadband or strong-motion far-field 

stations of the Global Seismic Network (GSN), modified 

Mercalli intensities (MMI) from “Did You Feel It” (DYFI) 

compiled by the USGS National Earthquake Information 

Center (http://earthquake.usgs.gov/earthquakes/eventpage/

usp000h60h#impact_dyfi), attenuation models based on 

the distance from the fault, and estimated site amplification 

effects. The ShakeMap (version 2) estimate of ground shaking 

from the earthquake overlain on the landslide concentrations 

from figure 2 is shown in figure 8. PGA patterns shown here 

are fairly crude estimates of the ground shaking. The relatively 

symmetrical “race track” shape of the PGA contours around 

the fault source are broadly consistent with the decrease in 

landslide concentration, but this rather generic estimate of the 

regional ground motion fails to explain local differences in 

landslide concentration that are likely controlled by variations 

in lithology, topography, and shaking.

Table 2. Areal distribution of earthquake-triggered landslides for different rock types in the study area.

[Square kilometers, km2]

Rock type Number of landslides Area of landslides

(km2

)

Area of rock type within 

study area

(km2

)

Percentage of rock 

type covered by

landslides

Alluvium 347 0.16 475.80 0.034

Calcareous 16,585 18.97 3,005.39 0.631

Volcanic 6,635 5.56 894.59 0.621

Total 23,567 24.69 4,375.78 1

0.564

1

The total percentage of rock type covered by landslides is the total landslide area divided by the total study area.
Figure 6. Detail of fault-slip model of Hayes and others (2010) for the Léogâne fault plane, with the figure also showing landslides and geology. Modeled fault plane dips 55° north. (Geologic units defined in fig. 1). 

°

°

Ems

Ems

72°75' 72°50'

18°50'18°25'

1

1

0.5

2 3

3

2.5

2.5

2

2

2

0.5

0.5

1

1

1

3

0.5

0.5

0.5

2.5

3.5

2.5

1.5

1.5

0.5

0.5

2 2

1.5

1.5

3.5

3

3

2

1.5 2.5

0.5

0.5

1

Ca

Cb

Cb

Cb

Cb

Cb

Cb

Cb

Cb

Ca

Cb

Cb

Cc

Cc

Qa

Qa

Cs

Cs

Cs

Cb

Cs

Cs

Cs

Cs

Ems

Ems

Ems

Ems

Ems

Ems

Ems

Ems

Ems

Ems

Ems

Ems

Ep

Ep

Ep

Ep

Ep

Ep

Ep

Ep

Ep

Ep

Mi

Mi

Mi

Mi

Mi

Mi Mi

Ms

P

P

P

P

P

P

Pi

Pi

Qa

Qa

Qa

Qa

Qac

O

O

O

O

O

O

Bainet

Rivière

Rivière

Rivière

Grande

Gauche

Rivière

Grosseline

de

Jacmel

Rivière

Momance

Canal du Sud 

Base map data from a variety of sources (see pamphlet), accessed fromhttp://hddsexplorer.usgs.gov/ between January 2013 and January 2014Projection: Universal Transverse Mercator, zone 18; World Geodetic System 1984 (WGS 84)False easting 500000.0, false northing 0.0, central meridian –75.0

ENRIQUILLO

Slip, in meters Geology

EXPLANATIO

Alluvium

Basalt and 

Limestone

Note: Colors may appear slightly different on tbecause of the application of a shaded relief b

0.2 to 0.70.7 to 1.01.0 to 1.5

1.5 to 2.42.4 to 3.43.4 to 4.5 

0 2.5 5 KILOMETERS0 2.5 5 MILES

FIGURE

AREA

Base from esri, accessed on Dec. 3, 2015 athttp://www.arcgis.com/home/webmap/viewer.html

HAITI

DOMINICAN

REPUBLIC

CUBA
Figure 7. Detail of fault-slip model of Symithe and others (2013) on map showing landslides and geology (geologic units defined in fig. 1). Eastern segment of modeled fault plane dips 65° north; western segment dips 71° north. 

.

72°75' 72°50'

18°50'

18°25'

1

1

4.5 4

4

3.5 3

1.5

2.5

2

2

0.5

2.5

2.5

1.5

2.5

2.5

2.5

2

2

2

0.5

1.5

1.5

1.5

1.5

1 1

0.5

1

2.5

1.5 1.5

1.5

2

3

3.5

3

3

2.5

1 1 3.5

1

1 

3.5

3

3

0.5

1.5 1

Cb

Cb

Cs Ep

Mi

Ca

Cb

Cb

Cb

Cb

Cb

Ca

Cb

Cb

Cc

Cc

Qa

Qa

Cs

Cs

Cs

Cb

Cs

Cs

Cs

Ems

Ems

Ems

Ems

Ems

Ems

Ems

Ems

Ems

Ems

Ems

Ems

Ep

Ep

Ep

Ep

Ep

Ep

Ep

Ep

Ep

Mi

Mi

Mi

Mi

Mi Mi

Ms

P

P

P

P

P

P

Pi

Pi

Qa

Qa

Qa

Qa

Qac

O

O

O

O

O

O

Cb

Canal du Sud

Base map data from a variety of sources (see pamphlet), accessed fromhttp://hddsexplorer.usgs.gov/ between January 2013 and January 2014Projection: Universal Transverse Mercator, zone 18; World Geodetic System 1984 (WGS 84)False easting 500000.0, false northing 0.0, central meridian –75.0

Bainet

Rivière

Rivière

Rivière

Grande

Gauche

de

Jacmel

Rivière

Momance

ENRIQUI

Slip, in meters Geology

EXPLANATIO

Alluvium

Basalt and 

Limestone

Note: Colors may appear slightly different on tbecause of the application of a shaded relief b

0.2 to 0.70.7 to 1.01.0 to 1.5

1.5 to 2.42.4 to 3.43.4 to 4.5 

FIGURE

AREA

Base from esri, accessed on Dec. 3, 2015 athttp://www.arcgis.com/home/webmap/viewer.html

HAITI

DOMINICAN

REPUBLIC

CUBA

0 2.5 5 KILOMETERS0 2.5 5 MILES
Figure 8. Map of landslide concentration overlain by ShakeMap contours of peak ground acceleration (PGA) from the earthquake (see http://ea

eventpage/gcmt20100112215310#impact_shakemap) (U.S. Geological Survey, 2010b).

Rivière

EX

Landslides tri by earthqua

Epicenter 

PGA (percent 

Major rivers

Roads

30

73°00' 72°75' 72°50' 72°25'

18°50'

18°25'

18°00'

Grand-Goâve

Petit-Goâve

Bainet

Jacmel

Port-au-Prince

Baie de

Port-au-Prince

CARIBBEAN SEA

30

40

40

40

60

60

80

80

70

70

70

50

50

50

90

Bainet

Rivière

Rivière

Rivière

Gauche Grande Rivière Grosseline

Rivière Froide

de Jacmel

Momance

Base map data from a variety of sources (see pamphlet), accessed from http://hddsexplorer.usgs.gov/ between January 2013 and January 2014Projection: Universal Transverse Mercator, zone 18; World Geodetic System 1984 (WGS 84); False easting 500000.0, false northing 0.0, central meridian –75.0

Canal du Sud

ENRIQUILLO-PLANTAIN GARDEN FAULT ZONE

0 5 10 15 20 KILOMETERS0 5 10 15 20 MILES

FIGURE

AREA

Base from esri, accessed on Dec. 3, 2015 athttp://www.arcgis.com/home/webmap/viewer.html

HAITI

DOMINICAN

REPUBLIC

CUBA
References Cited 13

Discussion

The relation of seismically triggered landslides to 

topography has been well known for decades. The locations 

of landslides triggered by earthquakes on steep slopes, ridges, 

and promontories have been documented in numerous publications (Harp and others, 1981; Harp and Keefer, 1990; Harp 

and Jibson, 1996; Ashford and others, 1997; Meunier and 

others, 2008). The distribution of landslides triggered by this 

earthquake follows similar general patterns.

The effect of material-property differences in rock and 

soil in influencing the patterns of seismically triggered landslides also has been well established (Harp and others, 1981; 

Harp and Keefer, 1990; Chigira and Yagi, 2006; Wang and 

others, 2007; Lee and others, 2008; Yagi and others, 2009; 

Dreyfus and others, 2013). We lack data on the shear strengths 

of the materials in our study area and thus cannot quantify this 

effect in this earthquake.

The effects of shaking variations on seismically triggered landslide distributions have been discussed in previous 

research with respect to both topographic amplification and 

the correlation of landslides with the hanging wall of a thrust 

earthquake (Harp and others, 1981; Abrahamson and Somerville, 1996; Harp and Jibson, 1996, 2002; Allen and others, 

1998; Shabestari and Yamazaki, 2003; Chang and others, 

2004). The effect of local variation of ground shaking during 

the Haiti earthquake on the landslide distribution cannot 

be assessed in detail because of the absence of any seismic 

instruments in the country at the time of the earthquake. 

However, finite-fault modeling and ShakeMap allow us to 

make some broad correlations between landslide distribution 

and ground motion.

Summary and Conclusions

Field reconnaissance shortly after the earthquake coupled 

with detailed examination of pre- and post-earthquake imagery 

have allowed us to produce a map showing 23,567 landslides 

triggered by the 2010 Haiti earthquake. In this report, we present a description and preliminary evaluation of the landslide 

distribution with respect to lithology, topography, models of 

fault slip, and strong shaking estimated by ShakeMap. Some 

general observations are as follows:

•	 Most of the landslides, as well as the highest local 

landslide concentrations, are within calcareous units 

(Ems and Cs), which have the greatest areal extent 

and the steepest slopes within the landslide-affected 

area. Overall landslide concentrations, however, are 

similar in calcareous and volcanic units. 

•	 Although some landslide sources for this earthquake 

are located on the crests of slopes, most occur within 

the steep drainages along rivers and at some distance 

below the ridge crests. 

•	 No clear relation is apparent between the landslide distribution and the fault-slip models. The greatest local 

landslide concentrations along the Rivière Momance 

near the EPGFZ are 10–12 km from the maximum 

fault slip in the fault-slip models; the westernmost 

high local landslide concentration south of GrandGoâve is about 8 km from the zones of maximum slip 

in the western part of the slip models.

•	 Unlike in many other thrust earthquakes, the large 

majority of landslides occurred on the footwall of the 

thrust fault. This is primarily because of the lack of 

susceptible slopes on the hanging wall.

•	 The lack of strong-motion instruments in Haiti precludes making a detailed analysis of the relation 

between landslide distribution and ground motion.

References Cited

Abrahamson, N.A., and Somerville, P.G., 1996, Effects of 

hanging wall and footwall on ground motions recorded during the Northridge earthquake: Bulletin of the Seismological Society of America, v. 86, no. 1B, p. S93–S99.

Allen, C.R., Brune, J.N., Cluff, L.S., and Barrows, A.G., 1998, 

Evidence for unusually strong near-field ground motion on 

the hanging wall of the San Fernando fault during the 1971 

earthquake: Seismological Research Letters, v. 69, no. 6, 

p. 524–531.

Ashford, S.A., Sitar, Nicholas, Lysmer, John, and Deng, Nan, 

1997, Topographic effects on the seismic response of steep 

slopes: Bulletin of the Seismological Society of America, 

v. 87, no. 3, p. 701–709.

Bureau des Mines et de l’Énergie, 2005, Carte Geologique 

de la République d’Haïti: République d’Haïti, Bureau des 

Mines et de l’Energie, scale 1:250,000 [In French]. [Also 

available at www.bme.gouv.ht/carte/notice.pdf.]

Calais, Eric, Freed, Andrew, Mattioli, Glen, Amelung, Falk, 

Jónsson, Sigurjón, Jansma, Pamela, Hong, S.-H., Dixon, 

Timothy, Prépetit, Claude, and Momplaiser, Roberte, 2010, 

Transpressional rupture of an unmapped fault during the 

2010 Haiti earthquake, Nature Geoscience, v. 3, p. 794–799.

Cavallo, E.A, Powell, Andrew, and Becerra, Oscar, 2010, 

Estimating the direct economic damage of the earthquake in 

Haiti: The Economic Journal, v. 120, is. 546, p. F298–F312, 

DOI: 10.1111/j.1468-0297.2010.02378.x.

Chang, T.Y., Cotton, Fabrice, Tsai, Y.B., and Angelier, 

Jacques, 2004, Quantification of hanging-wall effects 

on ground motion—Some insights from the 1999 ChiChi earthquake: Bulletin of the Seismological Society of 

America, v. 94, no. 6, p. 2186–2197.
14 Map of Landslides Triggered by the January 12, 2010, Haiti Earthquake

Chigira, Masahiro, and Yagi, Hiroshi, 2006, Geological and 

geomorphological characteristics of landslides triggered 

by the 2004 Mid Niigata Prefecture earthquake in Japan: 

Engineering Geology, v. 82, p. 202–221.

Dreyfus, Daniel, Rathje, E.M., and Jibson, R.W., 2013, The 

influence of different simplified sliding-block models and 

input parameters on regional predictions of seismic landslides triggered by the Northridge earthquake: Engineering 

Geology, v. 163, p. 41–54.

Gorum, Tolga, van Westen, C.J., Korup, Oliver, van der 

Meijde, Mark, Fan, Xuanmei, and van der Meer, F.D., 

2013, Complex rupture mechanism and topography control 

symmetry of mass-wasting pattern, 2010 Haiti earthquake: 

Geomorphology, v. 184, p. 127–138.

Harp, E.L., and Jibson, R.W., 1996, Landslides triggered by 

the Northridge, California, earthquake: Bulletin of the Seismological Society of America, v. 86, no. 1B, S319–S332.

Harp, E.L., and Jibson, R.W., 2002, Anomalous concentrations 

of seismically triggered rock falls in Pacoima Canyon—Are 

they caused by highly susceptible slopes or local amplification of seismic shaking?: Bulletin of the Seismological 

Society of America, v. 92, p. 3180–3189. 

Harp, E.L., and Keefer, D.K., 1990, Landslides triggered by 

the earthquake, in Rymer, M.J., and Ellsworth, W.L., eds., 

The Coalinga, California, earthquake of May 2, 1983: U.S. 

Geological Survey Professional Paper 1487, p. 335–347, 

1 pl. [Also available at http://pubs.er.usgs.gov/publication/

pp1487.]

Harp, E.L., Jibson, R.W., and Dart, R.L., 2013, The effect 

of complex fault rupture on the distribution of landslides 

triggered by the 12 January 2010, Haiti earthquake, in

Margottini, Claudio, Canuti, Paolo, and Sassa, Kyoji, eds., 

Landslide Science and Practice, Proceedings of the Second 

World Landslide Forum, v. 5, p. 157–161: Berlin, Heidelberg, Springer-Verlag, doi: 10.1007/978-3-642-31427-8_20.

Harp, E.L., Wilson, R.C., and Wieczorek, G.F., 1981, Landslides from the February 4, 1976, Guatemala earthquake: 

U.S. Geological Survey Professional Paper1204–A, p. 1–35, 

2 pl. [Also available at http://pubs.er.usgs.gov/publication/

pp1204A.]

Hayes, G.P., Briggs, R.W., Sladen, Anthony, Fielding, E.J., 

Prentice, Carol, Hudnut, Kenneth, Mann, Paul, Taylor, F.W., 

Crone, A.J., Gold, Ryan, Ito, Takeo, and Simons, Mark, 

2010, Complex rupture during the 12 January 2010 Haiti 

earthquake: Nature Geoscience, v. 3, p. 800–805.

Jibson, R.W., and Harp, E.L., 2011, Field reconnaissance 

report of landslides triggered by the January 12, 2010, Haiti 

earthquake: U.S. Geological Survey Open-File Report 

2011–1023, 18 p. [Also available at http://pubs.er.usgs.gov/

publication/ofr20111023.]

Keefer, D.K., 1984, Landslides caused by earthquakes: Geological Society of America Bulletin, v. 95, p. 406–421.

Kolbe, A.R., Hutson, R.A., Shannon, Harry, Trzinski, Eileen, 

Miles, Bart, Levitz, Naomi, Puccio, Marie, James, Leah, 

Noel, J.R., and Muggah, Robert, 2010, Mortality, crime, and 

access to basic needs before and after the Haiti earthquake: 

Medicine, Conflict, and Survival, v. 26, p. 281–297.

Lee, C.T., Huang, C.C., Lee, J.F., Pan, K.L., Lin, M.L., and 

Dong, J.J., 2008, Statistical approach to earthquake-induced 

landslide susceptibility: Engineering Geology, v. 100, 

p. 43–58.

Meunier, Patrick, Hovius, Niels, and Haines, J.A., 2008, Topographic site effects and the location of earthquake induced 

landslides: Earth and Planetary Science Letters, v. 275, 

p. 221–232.

Shabestari, K.T., and Yamazaki, Fumio, 2003, Near-fault 

spatial variation in strong ground motion due to rupture 

directivity and hanging wall effects from the Chi-Chi earthquake: Earthquake Engineering and Structural Dynamics: 

v. 32, p. 2197–2219.

Symithe, S.J., Calais, Eric, Haase, J.S., Freed, A.M., and 

Douilly, Roby, 2013, Coseismic slip distribution of the 

2010 M 7.0 Haiti earthquake and resulting stress changes 

on regional faults: Bulletin of the Seismological Society of 

America, v. 103, p. 2326–2343.

U.S. Geological Survey, ASTER 1 arc-second for scene 

ASTGDEMV2_0N18W073: U.S. Geological Survey 

Earth Resources Observation and Science (EROS) Center, 

accessed October 2011, at http://eros.usgs.gov/#/Find_Data/

Products_and_Data_Available/Aster. Link no longer active. 

The current link to find such data is as follows: http://

reverb.echo.nasa.gov/reverb/#utf8=%E2%9C%93&spatial_

map=satellite&spatial_type=rectangle.

U.S. Geological Survey, 2010a, Magnitude 7.0—Haiti region 

2010 January 12 21:53:10 UTC: U.S. Geological Survey, 

Earthquake hazards program. [Also available at http://

www.earthquake.usgs.gov/earthquakes/eqinthenews/2010/

us2010rja6/.]

U.S. Geological Survey, 2010b, ShakeMap, M7.0—Haiti 

region: U.S. Geological Survey, Earthquake hazards program. [Also available at http://earthquake.usgs.gov/earthquakes/eqinthenews/2010/us2010rja6/.]

Varnes, D.J., 1978, Slope movement types and processes, in

Schuster, R.L., and Krizek, R.J., eds., Landslides—Analysis 

and Control: Washington, D.C., National Research Council, Transportation Research Board, Special Report 176, 

p. 11–33. 

Wang, H.B., Sassa, Kyoji, and Xu, W.Y., 2007, Analysis of 

a spatial distribution of landslides triggered by the 2004 

Chuetsu earthquakes of Niigata Prefecture, Japan: Natural 

Hazards, v. 41, p. 43–60.
References Cited 15

Worden, C.B., Wald, D.J., Allen, T.I., Lin, K.-W., Garcia, 

Daniel, and Cua, Georgia, 2010, A revised ground-motion 

and intensity interpolation scheme for ShakeMap: Bulletin of the Seismological Society of America, v. 100, 

p. 3083–3096.

Xu, Chong, Shyu, J.B.H., and Xu, X.-W., 2014, Landslides 

triggered by the 12 January 2010 Mw 7.0 Port-au-Prince, 

Haiti, earthquake—Visual interpretation, inventory compiling and spatial distribution statistical analysis: Natural 

Hazards and Earth System Sciences, v. 14, p. 1789–1818.

Yagi, Hiroshi, Sato, Go, Higaki, Daisuke, Yamamoto, Miki, 

and Yamasaki, Takanari, 2009, Distribution and characteristics of landslides induced by the Iwate-Miyagi Nairiku 

earthquake in 2008 in Tohoku District, northeast Japan: 

Landslides, v. 6, p. 335–344.

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For more information concerning this publication, contact:

Center Director, USGS Geologic Hazards Science Center 

Box 25046, Mail Stop 966

Denver, CO 80225

(303) 273-8579

Harp and others—Map of Landslides Triggered by the January 12, 2010, Haiti Earthquake—Scientific Investigations Map 3353

ISSN 2329-132X (online)

http://dx.doi.org/10.3133/sim3353