Last 4 Major Earth Quake

8/10/2019 Last 4 Major Earth Quake

1/23

M6.9 - 43km ENE of Tambo, Peru (BETA)

2014-08-24 23:21:45 UTC

Legend

Epicenter

Nearby City

Plate Boundaries

GSHAP Hazard

ShakeMap

10 km

5 miPowered byLeaflet

Peru

14.586S, 73.578W

Depth: 101.0km (62.8mi)

Event Time

1. 2014-08-24 23:21:45 UTC2. 2014-08-24 18:21:45 UTC-05:00 at epicenter3. 2014-08-25 04:51:45 UTC+05:30 system time

Location
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2/23

14.586S 73.578W depth=101.0km (62.8mi)

Nearby Cities

1. 43km (27mi) ENE of Tambo, Peru

2. 61km (38mi) ENE of Puquio, Peru3. 105km (65mi) S of Andahuaylas, Peru4. 129km (80mi) SW of Abancay, Peru5. 467km (290mi) SE of Lima, Peru

Tectonic Summary

Seismotectonics of South America (Nazca Plate Region)

The South American arc extends over 7,000 km, from the Chilean margin triple junction offshore

of southern Chile to its intersection with the Panama fracture zone, offshore of the southern coast

of Panama in Central America. It marks the plate boundary between the subducting Nazca plateand the South America plate, where the oceanic crust and lithosphere of the Nazca plate begin

their descent into the mantle beneath South America. The convergence associated with this

subduction process is responsible for the uplift of the Andes Mountains, and for the activevolcanic chain present along much of this deformation front. Relative to a fixed South America

plate, the Nazca plate moves slightly north of eastwards at a rate varying from approximately 80

mm/yr in the south to approximately 65 mm/yr in the north. Although the rate of subductionvaries little along the entire arc, there are complex changes in the geologic processes along the

subduction zone that dramatically influence volcanic activity, crustal deformation, earthquake

generation and occurrence all along the western edge of South America.

Most of the large earthquakes in South America are constrained to shallow depths of 0 to 70 kmresulting from both crustal and interplate deformation. Crustal earthquakes result fromdeformation and mountain building in the overriding South America plate and generate

earthquakes as deep as approximately 50 km. Interplate earthquakes occur due to slip along the

dipping interface between the Nazca and the South American plates. Interplate earthquakes inthis region are frequent and often large, and occur between the depths of approximately 10 and60 km. Since 1900, numerous magnitude 8 or larger earthquakes have occurred on this

subduction zone interface that were followed by devastating tsunamis, including the 1960 M9.5

earthquake in southern Chile, the largest instrumentally recorded earthquake in the world. Othernotable shallow tsunami-generating earthquakes include the 1906 M8.5 earthquake near

Esmeraldas, Ecuador, the 1922 M8.5 earthquake near Coquimbo, Chile, the 2001 M8.4

Arequipa, Peru earthquake, the 2007 M8.0 earthquake near Pisco, Peru, and the 2010 M8.8Maule, Chile earthquake located just north of the 1960 event.

Large intermediate-depth earthquakes (those occurring between depths of approximately 70 and

300 km) are relatively limited in size and spatial extent in South America, and occur within theNazca plate as a result of internal deformation within the subducting plate. These earthquakes

generally cluster beneath northern Chile and southwestern Bolivia, and to a lesser extent beneath

northern Peru and southern Ecuador, with depths between 110 and 130 km. Most of these


3/23

earthquakes occur adjacent to the bend in the coastline between Peru and Chile. The most recent

large intermediate-depth earthquake in this region was the 2005 M7.8 Tarapaca, Chile

earthquake.

Earthquakes can also be generated to depths greater than 600 km as a result of continued internal

deformation of the subducting Nazca plate. Deep-focus earthquakes in South America are notobserved from a depth range of approximately 300 to 500 km. Instead, deep earthquakes in this

region occur at depths of 500 to 650 km and are concentrated into two zones: one that runs

beneath the Peru-Brazil border and another that extends from central Bolivia to centralArgentina. These earthquakes generally do not exhibit large magnitudes. An exception to this

was the 1994 Bolivian earthquake in northwestern Bolivia. This M8.2 earthquake occurred at a

depth of 631 km, which was until recently the largest deep-focus earthquake instrumentally

recorded (superseded in May 2013 by a M8.3 earthquake 610 km beneath the Sea of Okhotsk,Russia), and was felt widely throughout South and North America.

Subduction of the Nazca plate is geometrically complex and impacts the geology and seismicity

of the western edge of South America. The intermediate-depth regions of the subducting Nazcaplate can be segmented into five sections based on their angle of subduction beneath the South

America plate. Three segments are characterized by steeply dipping subduction; the other two bynear-horizontal subduction. The Nazca plate beneath northern Ecuador, southern Peru to

northern Chile, and southern Chile descend into the mantle at angles of 25 to 30. In contrast,

the slab beneath southern Ecuador to central Peru, and under central Chile, is subducting at a

shallow angle of approximately 10 or less. In these regions of flat-slab subduction, the Nazcaplate moves horizontally for several hundred kilometers before continuing its descent into the

mantle, and is shadowed by an extended zone of crustal seismicity in the overlying South

America plate. Although the South America plate exhibits a chain of active volcanism resultingfrom the subduction and partial melting of the Nazca oceanic lithosphere along most of the arc,

these regions of inferred shallow subduction correlate with an absence of volcanic activity.

Instrumental Intensity


4/23

PAGER

Impact Estimates

Estimated Fatalities


5/23

Estimated Economic Losses

Green alert for shaking-relatedfatalities and economic losses. There is a low likelihood of casualties and damage.

Estimated Population Exposure to Earthquake Shaking

EstimatedModified

Mercalli

Intensity

I II-III IV V VI VII VIII IX X

Est. Population

Exposure--*

2,837k*

3,047k

254k 15k 0k 0k 0k 0k

Perceived

Shaking

Not

FeltWeak Light

Moder

ateStrong Very Strong Severe

Violen

t

Extre

me

Potenti

al

Structure

Damag

e

Resistan

t

none

none noneV.Light

Light ModerateModerate/Heavy

HeavyV.Heavy

Vulnera

ble

non

enone none Light

Moder

ate

Moderate/He

avyHeavy

V.Hea

vy

V.Hea

vy

*Estimated exposure only includes population within calculated shake map area. (k = x1,000)

Population Exposure
http://comcat.cr.usgs.gov/learning/topics/mercalli.phphttp://comcat.cr.usgs.gov/learning/topics/mercalli.phphttp://comcat.cr.usgs.gov/learning/topics/mercalli.phphttp://comcat.cr.usgs.gov/learning/topics/mercalli.phphttp://comcat.cr.usgs.gov/product/losspager/usb000s5x1/us/1408925941057/alertecon.pdfhttp://comcat.cr.usgs.gov/product/losspager/usb000s5x1/us/1408925941057/alertfatal.pdfhttp://comcat.cr.usgs.gov/product/losspager/usb000s5x1/us/1408925941057/alertecon.pdfhttp://comcat.cr.usgs.gov/product/losspager/usb000s5x1/us/1408925941057/alertfatal.pdfhttp://comcat.cr.usgs.gov/learning/topics/mercalli.phphttp://comcat.cr.usgs.gov/learning/topics/mercalli.phphttp://comcat.cr.usgs.gov/learning/topics/mercalli.php


6/23

Population per 1 sq. km. from LandScan

Structure Information Summary

Overall, the population in this region resides in structures that are vulnerable to earthquakeshaking, though some resistant structures exist.

Secondary Effects

Recent earthquakes in this area have caused secondary hazards such as tsunamis and landslides

that might have contributed to losses.

Selected Cities Exposed

fromGeoNames Database of Cities with 1,000 or more residents.

MMI City Population

VI Incuyo


7/23

MMI City Population

V Tambo 5k

V Pampachiri


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Parameter Value Uncertainty

Number of Stations UsedNot Specified

Number of Phases Used 155

Minimum Distance 455.9 km (4.10)

Travel Time Residual 1.32 secAzimuthal Gap 23

Review Status MANUAL

Event ID usb000s5x1


9/23

M6.9 - Federated States of Micronesia region

(BETA) 2014-08-03 00:22:03 UTC

Summary

Location and Magnitude contributed by:USGS National Earthquake Information Center

General

USGS Topography Open Street Map Open Aerial Map

USGS Plate Boundaries ShakeMap Nearby Cities Earthquake Location

Legend

Epicenter

Nearby City

Plate Boundaries

GSHAP Hazard

ShakeMap

10 km

5 mi

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10/23

0.837N, 146.169E

Depth: 12.3km (7.6mi)

Event Time

1. 2014-08-03 00:22:03 UTC2. 2014-08-03 10:22:03 UTC+10:00 at epicenter3. 2014-08-03 05:52:03 UTC+05:30 system time

Location

0.837N 146.169E depth=12.3km (7.6mi)

Nearby Cities

1. 339km (211mi) NNW of Lorengau, Papua New Guinea

2. 561km (349mi) NNE of Wewak, Papua New Guinea3. 638km (396mi) NW of Kavieng, Papua New Guinea4. 666km (414mi) NE of Vanimo, Papua New Guinea5. 1142km (710mi) N of Port Moresby, Papua New Guinea

Related Links

Additional earthquake information for Papua New Guinea

View location in Google Maps

Tectonic Summary

Seismotectonics of the New Guinea Region and Vicinity

The Australia-Pacific plate boundary is over 4000 km long on the northern margin, from the

Sunda (Java) trench in the west to the Solomon Islands in the east. The eastern section is over

2300 km long, extending west from northeast of the Australian continent and the Coral Sea untilit intersects the east coast of Papua New Guinea. The boundary is dominated by the general

northward subduction of the Australia plate.

Along the South Solomon trench, the Australia plate converges with the Pacific plate at a rate ofapproximately 95 mm/yr towards the east-northeast. Seismicity along the trench is dominantly

related to subduction tectonics and large earthquakes are common: there have been 13 M7.5+

earthquakes recorded since 1900. On April 1, 2007, a M8.1 interplatemegathrust earthquakeoccurred at the western end of the trench, generating a tsunami and killing at least 40 people.

This was the third M8.1 megathrust event associated with this subduction zone in the past

century; the other two occurred in 1939 and 1977.
http://earthquake.usgs.gov/earthquakes/world/index.php?regionID=70http://earthquake.usgs.gov/earthquakes/world/index.php?regionID=70http://maps.google.com/maps?q=0.8371+146.1691%28M6.9++-+Federated+States+of+Micronesia+region+-+2014-08-03+00%3A22%3A03+UTC%29&ll=0.8371,146.1691&spn=2,2&f=d&t=h&hl=ehttp://maps.google.com/maps?q=0.8371+146.1691%28M6.9++-+Federated+States+of+Micronesia+region+-+2014-08-03+00%3A22%3A03+UTC%29&ll=0.8371,146.1691&spn=2,2&f=d&t=h&hl=ehttp://maps.google.com/maps?q=0.8371+146.1691%28M6.9++-+Federated+States+of+Micronesia+region+-+2014-08-03+00%3A22%3A03+UTC%29&ll=0.8371,146.1691&spn=2,2&f=d&t=h&hl=ehttp://earthquake.usgs.gov/earthquakes/world/index.php?regionID=70


11/23

Further east at the New Britain trench, the relative motions of several microplates surrounding

the Australia-Pacific boundary, including north-south oriented seafloor spreading in the

Woodlark Basin south of the Solomon Islands, maintain the general northward subduction ofAustralia-affiliated lithosphere beneath Pacific-affiliated lithosphere. Most of the large and great

earthquakes east of New Guinea are related to this subduction; such earthquakes are particularly

concentrated at the cusp of the trench south of New Ireland. 33 M7.5+ earthquakes have beenrecorded since 1900, including three shallow thrust fault M8.1 events in 1906, 1919, and 2007.

The western end of the Australia-Pacific plate boundary is perhaps the most complex portion ofthis boundary, extending 2000 km from Indonesia and the Banda Sea to eastern New Guinea.

The boundary is dominantly convergent along an arc-continent collision segment spanning the

width of New Guinea, but the regions near the edges of the impinging Australia continental

margin also include relatively short segments of extensional, strike-slip and convergentdeformation. The dominant convergence is accommodated by shortening and uplift across a 250-

350 km-wide band of northern New Guinea, as well as by slow southward-verging subduction of

the Pacific plate north of New Guinea at the New Guinea trench. Here, the Australia-Pacific

plate relative velocity is approximately 110 mm/yr towards the northeast, leading to the 2-8mm/yr uplift of the New Guinea Highlands.

Whereas the northern band of deformation is relatively diffuse east of the Indonesia-Papua New

Guinea border, in western New Guinea there are at least two small (


12/23

in intermediate depth seismicity under Timor and seismic mechanisms that indicate an eastward

propagating tear in the descending slab as the negatively buoyant oceanic lithosphere detaches

from positively buoyant continental lithosphere. On the surface, GPS measurements indicate thatthe region around Timor is currently no longer connected to the Eurasia plate, but instead is

moving at nearly the same velocity as the Australia plate, another consequence of collision.

Large earthquakes in eastern Indonesia occur frequently but interplatemegathrust events related

to subduction are rare; this is likely due to the disconnection of the descending oceanic slab from

the continental margin. There have been 9 M7.5+ earthquakes recorded from the Kai Islands toSumba since 1900. The largest was the great Banda Sea earthquake of 1938 (M8.5) an

intermediate depth thrust faulting event that did not cause significant loss of life.

More information on regional seismicity and tectonics

Additional Data Contributors

Alaska Tsunami Warning Center Pacific Tsunami Warning Center

ShakeMap

Contributed byUSGS National Earthquake Information Center


ShakeMap Intensity Image

PGA (%g)

ShakeMap PGA Image

PGV (cm/s)

ShakeMap PGV Image

PSA 0.3s (%g)

Spectral Response - 0.3 Second Period

PSA 1.0s (%g)


PSA 3.0s (%g)
http://pubs.usgs.gov/of/2010/1083/h/http://pubs.usgs.gov/of/2010/1083/h/http://wcatwc.arh.noaa.gov/http://wcatwc.arh.noaa.gov/http://ptwc.weather.gov/http://ptwc.weather.gov/http://earthquake.usgs.gov/regional/neic/http://earthquake.usgs.gov/regional/neic/http://earthquake.usgs.gov/regional/neic/http://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/intensity.jpg#usemap=shakemap_imagemaphttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/intensity.jpg#usemap=shakemap_imagemaphttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/pga.jpg#usemap=shakemap_imagemaphttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/pga.jpg#usemap=shakemap_imagemaphttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/pgv.jpg#usemap=shakemap_imagemaphttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/pgv.jpg#usemap=shakemap_imagemaphttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/psa03.jpg#usemap=shakemap_imagemaphttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/psa03.jpg#usemap=shakemap_imagemaphttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/psa10.jpg#usemap=shakemap_imagemaphttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/psa10.jpg#usemap=shakemap_imagemaphttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/psa10.jpg#usemap=shakemap_imagemaphttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/psa03.jpg#usemap=shakemap_imagemaphttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/pgv.jpg#usemap=shakemap_imagemaphttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/pga.jpg#usemap=shakemap_imagemaphttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/intensity.jpg#usemap=shakemap_imagemaphttp://earthquake.usgs.gov/regional/neic/http://ptwc.weather.gov/http://wcatwc.arh.noaa.gov/http://pubs.usgs.gov/of/2010/1083/h/


13/23


Uncertainty

ShakeMap Uncertainty Image

Station List

Text

XMLScientific Background on the ShakeMap Process

PAGER

Pager XMLDownload Alert PDF

Impact Estimates


Histogram of Estimated Fatalities


Histogram of Estimated Economic LossesPopulation Exposure Map

Historic Seismicity

Historic Earthquakes

City Exposure List

See PAGER XML link (above).

PAGER content is automatically generated, and only considers losses due to structuraldamage. Limitations of input data, shaking estimates, and loss models may add uncertainty.

PAGER results are generally available within 30 minutes of the earthquakes occurrence.However, information on the extent of shaking will be uncertain in the minutes and hours

following an earthquake and typically improves as additional sensor data and reported intensities

are acquired and incorporated into models of the earthquakes source. Users of PAGER estimatesshould account for uncertainty and always seek the most current PAGER release for any

earthquake.
http://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/psa30.jpg#usemap=shakemap_imagemaphttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/psa30.jpg#usemap=shakemap_imagemaphttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/sd.jpg#usemap=shakemap_imagemaphttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/sd.jpg#usemap=shakemap_imagemaphttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/stationlist.txthttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/stationlist.txthttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/stationlist.xmlhttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/stationlist.xmlhttp://comcat.cr.usgs.gov/research/shakemap/http://comcat.cr.usgs.gov/research/shakemap/http://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/pager.xmlhttp://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/pager.xmlhttp://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/alertfatal.pdf#thumb=http://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/alertfatal_small.pnghttp://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/alertfatal.pdf#thumb=http://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/alertfatal_small.pnghttp://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/alertecon.pdf#thumb=http://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/alertecon_small.pnghttp://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/alertecon.pdf#thumb=http://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/alertecon_small.pnghttp://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/exposure.png#thumb=http://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/exposure_small.pnghttp://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/exposure.png#thumb=http://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/exposure_small.pnghttp://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/historical_events.pnghttp://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/historical_events.pnghttp://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/historical_events.pnghttp://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/exposure.png#thumb=http://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/exposure_small.pnghttp://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/alertecon.pdf#thumb=http://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/alertecon_small.pnghttp://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/alertfatal.pdf#thumb=http://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/alertfatal_small.pnghttp://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/pager.xmlhttp://comcat.cr.usgs.gov/product/losspager/usb000rzki/us/1409024156450/pager.xmlhttp://comcat.cr.usgs.gov/research/shakemap/http://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/stationlist.xmlhttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/stationlist.txthttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/sd.jpg#usemap=shakemap_imagemaphttp://comcat.cr.usgs.gov/product/shakemap/usb000rzki/us/1409023921495/download/psa30.jpg#usemap=shakemap_imagemap


14/23

Scientific Background on the PAGER Process

Read Additional PAGER Disclaimers

Did You Feel It?Tell Us!


Tell Us!

Did you feel this earthquake?Tell Us!

Intensity Maps

Intensity Map

Graphs

Intensity vs. Distance

Responses vs. Time

Responses

Response Data (489)Scientific Background on the Did You Feel It? Process

Scientific


Summary

Preferred Location Parameters


Magnitude 6.9 mww Not Specified

Location 0.837N, 146.169E Not Specified

Depth 12.3 km 2.6 km




Travel Time Residual 0.95 sec

Azimuthal Gap 12
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15/23


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M7.9 - 21km SE of Little Sitkin Island,

Alaska (BETA) 2014-06-23 20:53:09 UTC

PAGER - GREENShakeMap - VIIIDYFI? - VI
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16/23

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17/23

5 km

5 miPowered byLeaflet

51.830N, 178.750E

Depth: 109.0km (67.7mi)

Event Time

1. 2014-06-23 20:53:09 UTC2. 2014-06-23 11:53:09 UTC-09:00 at epicenter3. 2014-06-24 02:23:09 UTC+05:30 system time

Location

51.830N 178.750E depth=109.0km (67.7mi)

Nearby Cities

1. 21km (13mi) SE of Little Sitkin Island, Alaska2. 1369km (851mi) E of Petropavlovsk-Kamchatskiy, Russia3. 1386km (861mi) E of Yelizovo, Russia4. 1386km (861mi) E of Vilyuchinsk, Russia5. 2955km (1836mi) W of Whitehorse, Canada

Related Links

Additional earthquake information for United States

Additional earthquake information for Alaska

Earthquake Summary Poster

View location in Google Maps

Tectonic Summary

The June 23, 2014 20:53 UTC earthquake in the Aleutian Islands, Alaska, occurred as the result

of oblique normal faulting at moderate depths. At the location of this event, the Pacific platesubducts northward beneath the North America plate at a rate of approximately 59 mm/yr. The

mechanism, location, and depth of the June 23 event indicate that the earthquake likely occurredwithin the subducting Pacific plate, several kilometers beneath the slab interface.

The locus of the June 23 event is a very seismically active region, with 26 events of M 7 orgreater having occurred within 250 km since 1900. Notable events include an M 8.4 in 1906, M
http://leafletjs.com/http://leafletjs.com/http://leafletjs.com/http://earthquake.usgs.gov/earthquakes/world/index.php?regionID=24http://earthquake.usgs.gov/earthquakes/world/index.php?regionID=24http://earthquake.usgs.gov/earthquakes/states/index.php?regionID=3http://earthquake.usgs.gov/earthquakes/states/index.php?regionID=3http://earthquake.usgs.gov/earthquakes/eqarchives/poster/2014/20140623.phphttp://earthquake.usgs.gov/earthquakes/eqarchives/poster/2014/20140623.phphttp://maps.google.com/maps?q=51.8297+178.75%28M7.9++-+21km+SE+of+Little+Sitkin+Island%2C+Alaska+-+2014-06-23+20%3A53%3A09+UTC%29&ll=51.8297,178.75&spn=2,2&f=d&t=h&hl=ehttp://maps.google.com/maps?q=51.8297+178.75%28M7.9++-+21km+SE+of+Little+Sitkin+Island%2C+Alaska+-+2014-06-23+20%3A53%3A09+UTC%29&ll=51.8297,178.75&spn=2,2&f=d&t=h&hl=ehttp://maps.google.com/maps?q=51.8297+178.75%28M7.9++-+21km+SE+of+Little+Sitkin+Island%2C+Alaska+-+2014-06-23+20%3A53%3A09+UTC%29&ll=51.8297,178.75&spn=2,2&f=d&t=h&hl=ehttp://earthquake.usgs.gov/earthquakes/eqarchives/poster/2014/20140623.phphttp://earthquake.usgs.gov/earthquakes/states/index.php?regionID=3http://earthquake.usgs.gov/earthquakes/world/index.php?regionID=24http://leafletjs.com/


18/23

8.7 in 1965, and an M 7.9 in 1996 . Unlike the June 23 event, many of these events occurred at

shallower depths, likely along the plate boundary interface.

Seismotectonics of Alaska

The Aleutian arc extends approximately 3,000 km from the Gulf of Alaska in the east to theKamchatka Peninsula in the west. It marks the region where the Pacific plate subducts into the

mantle beneath the North America plate. This subduction is responsible for the generation of the

Aleutian Islands and the deep offshore Aleutian Trench.

The curvature of the arc results in a westward transition of relative plate motion from trench-normal (i.e., compressional) in the east to trench-parallel (i.e., translational) in the west,

accompanied by westward variations in seismic activity, volcanism, and overriding plate

composition. The Aleutian arc is generally divided into three regions: the western, central, and

eastern Aleutians. Relative to a fixed North America plate, the Pacific plate is moving northwestat a rate that increases from roughly 60 mm/yr at the arc's eastern edge to 76 mm/yr near its

western terminus. The eastern Aleutian arc extends from the Alaskan Peninsula in the east to theFox Islands in the west. Motion along this section of the arc is characterized by arc-perpendicular

convergence and Pacific plate subduction beneath thick continental lithosphere. This regionexhibits intense volcanic activity and has a history of megathrust earthquakes.

The central Aleutian arc extends from the Andreanof Islands in the east to the Rat Islands in thewest. Here, motion is characterized by westward-increasing oblique convergence and Pacific

plate subduction beneath thin oceanic lithosphere. Along this portion of the arc, the Wadati-

Benioff zone is well defined to depths of approximately 200 km. Despite the obliquity ofconvergence, active volcanism and megathrust earthquakes are also present along this margin.

The western Aleutians, stretching from the western end of the Rat Islands in the east to theCommander Islands, Russia, in the west, is tectonically different from the central and eastern

portions of the arc. The increasing component of transform motion between the Pacific and

North America plates is evidenced by diminishing active volcanism; the last active volcano islocated on Buldir Island, in the far western portion of the Rat Island chain. Additionally, this

portion of the subduction zone has not hosted large earthquakes or megathrust events in recorded

history. Instead, the largest earthquakes in this region are generally shallow, predominantlystrike-slip events with magnitudes between M5-6. Deeper earthquakes do occur, albeit rather

scarcely and with small magnitudes (M


19/23

The Aleutian arc is a seismically active region, evidenced by the many moderate to large

earthquakes occurring each year. Since 1900, this region has hosted twelve large earthquakes

(M>7.5) including the May 7, 1986 M8.0 Andreanof Islands, the June 10, 1996 M7.9 AndreanofIslands, and the November 17, 2003 M7.8 Rat Islands earthquakes. Six of these great

earthquakes (M8.3 or larger) have occurred along the Aleutian arc that together have ruptured

almost the entire shallow megathrust contact. The first of these major earthquakes occurred onAugust 17, 1906 near the island of Amchitka (M8.3) in the western Aleutian arc. However,unlike the other megathrust earthquakes along the arc, this event is thought to have been an

intraplate event occurring in the shallow slab beneath the subduction zone interface.

The first megathrust event along the arc during the 20th century was the November 10, 1938

M8.6 Shumagin Island earthquake. This event ruptured an approximately 300 km long stretch of

the arc from the southern end of Kodiak Island to the northern end of the Shumagin Islands andgenerated a small tsunami that was recorded as far south as Hawaii.

The April 1, 1946 M8.6 Unimak Island earthquake, located in the central Aleutian arc, was

characterized by slow rupture followed by a devastating Pacific-wide tsunami that was observedas far south as the shores of Antarctica. Although damage from earthquake shaking was not

severe locally, tsunami run-up heights were recorded as high as 42 m on Unimak Island andtsunami waves in Hilo, Hawaii also resulted in casualties. The slow rupture of this event has

made it difficult to constrain the focal mechanism and depth of the earthquake, though it is

thought to have been an interplate thrust earthquake.

The next megathrust earthquake occurred along the central portion of the Aleutian arc near the

Andreanof Islands on March 9, 1957, with a magnitude of M8.6. The rupture length of this event

was approximately 1200 km, making it the longest observed aftershock zone of all the historicAleutian arc events. Although only limited seismic data from this event are still available,

significant damage and tsunamis were observed on the islands of Adak and Unimak with tsunamiheights of approximately 13 m.

The easternmost megathrust earthquake was the March 28, 1964 M9.2 Prince William Sound

earthquake, currently the second largest recorded earthquake in the world. The event had arupture length of roughly 700 km extending from Prince William Sound in the northeast to the

southern end of Kodiak Island in the southwest. Extensive damage was recorded in Kenai,

Moose Pass, and Kodiak but significant shaking was felt over a large region of Alaska, parts ofwestern Yukon Territory, and British Columbia, Canada. Property damage was the largest in

Anchorage, as a result of both the main shock shaking and the ensuing landslides. This

megathrust earthquake also triggered a devastating tsunami that caused damage along the Gulf of

Alaska, the West Coast of the United States, and in Hawaii.

The westernmost Aleutians megathrust earthquake followed a year later on February 4, 1965.

This M8.7 Rat Islands earthquake was characterized by roughly 600 km of rupture. Although thisevent is quite large, damage was low owing to the region's remote and sparsely inhabited

location. A relatively small tsunami was recorded throughout the Pacific Ocean with run-up

heights up to 10.7 m on Shemya Island and flooding on Amchitka Island.


20/23

Although the Aleutian arc is highly active, seismicity is rather discontinuous, with two regions

that have not experienced a large (M>8.0) earthquake in the past century: the Commander

Islands in the western Aleutians and the Shumagin Islands in the east. Due to the dominantlytransform motion along the western arc, there is potential that the Commander Islands will

rupture in a moderate to large strike-slip earthquake in the future. The Shumagin Islands region

may also have high potential for hosting a large rupture in the future, though it has beensuggested that little strain is being accumulated along this section of the subduction zone, andthus associated hazards may be reduced.

East of the Aleutian arc along the Gulf of Alaska, crustal earthquakes occur as a result

transmitted deformation and stress associated with the northwestward convergence of the Pacific

plate that collides a block of oceanic and continental material into the North America plate. In

2002, the Denali Fault ruptured in a sequence of earthquakes that commenced with the October23 M6.7 Nenana Mountain right-lateral strike-slip earthquake and culminated with the

November 3, M7.9 Denali earthquake which started as a thrust earthquake along a then

unrecognized fault and continued with a larger right-lateral strike-slip event along the Denali and

Totschunda Faults.

More information on regional seismicity and tectonics

Additional Data Contributors

Alaska Earthquake Information Center

Pacific Tsunami Warning Center

Alaska Tsunami Warning Center

ShakeMap



ShakeMap Intensity Image

PGA (%g)

ShakeMap PGA Image

PGV (cm/s)

ShakeMap PGV Image

PSA 0.3s (%g)

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21/23

PSA 1.0s (%g)


PSA 3.0s (%g)


Uncertainty

ShakeMap Uncertainty Image

Station List

Text

XML

Scientific Background on the ShakeMap Process

PAGER

Pager XMLDownload Alert PDF

Impact Estimates


Histogram of Estimated Fatalities


Histogram of Estimated Economic Losses

Population Exposure Map

Historic Seismicity

Historic Earthquakes

City Exposure List

See PAGER XML link (above).

PAGER content is automatically generated, and only considers losses due to structural

damage. Limitations of input data, shaking estimates, and loss models may add uncertainty.

PAGER results are generally available within 30 minutes of the earthquakes occurrence.

However, information on the extent of shaking will be uncertain in the minutes and hours
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following an earthquake and typically improves as additional sensor data and reported intensities

are acquired and incorporated into models of the earthquakes source. Users of PAGER estimates

should account for uncertainty and always seek the most current PAGER release for anyearthquake.

Scientific Background on the PAGER ProcessRead Additional PAGER Disclaimers

Did You Feel It?Tell Us!


Tell Us!

Did you feel this earthquake?Tell Us!

Intensity Maps

Intensity Map

Graphs

Intensity vs. DistanceResponses vs. Time

Responses

Response Data (947)

Scientific Background on the Did You Feel It? Process

Scientific


Summary

Preferred Location Parameters


Magnitude 7.9 mww Not Specified

Location 51.830N, 178.750E Not Specified

Depth 109.0 km 1.8 km

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Travel Time Residual 0.71 sec

Azimuthal Gap 22Review Status MANUAL

Event ID usc000rki5

Documents

Last 4 Major Earth Quake