Registro de Aceleraciones 2013

7/27/2019 Registro de Aceleraciones 2013

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PAGINA DEL IGP -REGISTRO DE ACELERACIONES 2013

*DATOS ADJUNTOS EN EL CD DE LOS 5 ULTIMOS REGISTROS, PERO COMOSE OBSERVA LOS SISMOS

DE AMYOR INTENSIDAD FUERON EN TOQUEPALA Y YAUCA

Intensidad

Mxima

06/01/2013 14:34:51 -17,47 -72,41 42 4,5 II Mollendo TOQ15/01/2013 22:34:44 -5,89 -81,05 30 4,9 III Sechura

11/02/2013 13:59:11 -10,42 - 74,47 110 4,6 II Oxapampa

22/02/2013 20:15:21 -15,84 -71,81 5 4,9 IV Maca TOQYCA

22/02/2013 21:01:46 -15,87 -71,81 8 5,2 V Maca TOQYCA

22/02/2013 21:50:45 -15,9 -71,8 7 5,2 V Maca TOQYCA

23/02/2013 20:08:17 -15,84 -71,8 9 4,6 III Maca

09/03/2013 4:40:25 -10,38 -78,69 56 4,5 II Huarmey YLS

14/03/2013 15:50:45 -15,8 -71,85 6 4,5 III Maca TOQ

17/03/2013 17:35:51 -8,91 -80,35 57 4,5 II Trujillo YLS

19/03/2013 5:53:44 -9,84 -75,32 146 4,5 II Pozuzo

19/03/2013 23:06:28 -13,16 -76,39 69 4,6 III-IV Lunahuan YCAYLS

23/03/2013 22:37:32 -15,85 -71,76 10 4,6 III Maca TOQ

27/03/2013 20:59:27 -11,02 -74,21 123 4,9 II Satipo

30/03/2013 17:30:46 -9,57 -79,42 17 5,4 IV Chimbote YLS

06/04/2013 8:49:26 -8,91 -79,06 65 4,5 III Chimbote YLS

07/04/2013 8:40:34 -7,99 -79,82 63 4,8 III Trujillo YLS

07/04/2013 20:40:48 -13,67 -76,5 46 4,7 III Chincha Alta UICA

07/04/2013 22:36:53 -17,28 -72,07 52 4,5 III Mollendo TOQ

10/04/2013 16:20:22 -10,77 -75,41 140 5 III Oxapampa HUAPUC

05/05/2013 13:18:56 -9,52 -79,23 52 5,2 III Chimbote YLS

13/05/2013 13:54:04 -8,38 -80,4 38 4,8 II San Pedro de YLS

14/05/2013 23:39:15 -15,69 -73,32 104 5,6 5,8 III Caravel TAMTOQUICAYC

A

17/05/2013 16:29:49 -10,57 -75,09 32 4,5 III Oxapampa HUA

21/05/2013 23:02:42 -13,87 -72,7 90 5,7 5,8 IV Abancay TAM

02/06/2013 10:46:24 -14,56 -75,7 72 4,6 III Ica UICA

04/06/2013 10:33:06 -17,77 -69,96 177 4,6 II Tarata TOQ

18/06/2013 18:39:59 -11,98 -77,64 44 4,8 III-IV Callao ANC

30/06/2013 2:32:55 -14,82 -75,97 46 4,8 II Ica UICA

30/06/2013 16:39:11 -14,85 -75,62 41 4,6 III Palpa UICA

12/07/2013 10:29:42 -6,01 -75,42 37 4,5 II Yurimaguas

15/07/2013 22:35:46 -9,78 -74,73 135 5,1 II-III Pozuzo PUC

16/07/2013 9:27:37 -15,67 -71,91 20 4,5 III Cabanaconde

17/07/2013 2:37:42 -15,75 -72,05 9 6 6 V-VI Huambo TOQ

17/07/2013 12:59:16 -5,95 -76,16 74 4,6 II Lamas

23/07/2013 9:48:50 -9,08 -78,9 69 4,7 III-IV Chimbote YLS

25/07/2013 2:07:20 -15,75 -72,01 7 4,5 II Huambo

31/07/2013 10:25:19 -8,62 -79,95 44 4,5 II Trujillo YLS

31/07/2013 10:28:08 -5,12 -80,74 44 4,7 III-IV Piura UDP

02/08/2013 3:21:03 -17,89 -69,98 120 4,6 II Tacna LYA

08/08/2013 15:21:42 -17,89 -70,76 60 4,5 II-III Tacna LYA

12/08/2013 2:27:55 -6,32 -80,15 58 4,5 II Olmos

12/08/2013 9:49:30 -5,23 -81,67 13 5,8 IV Paita UDP

20/08/2013 1:16:21 -8,59 -79,72 36 4,8 III Trujillo CBT

Mw Localidad Estacin

REGISTRO DE ACELERACIN PARA SISMOS SENSIBLES EN EL 2013

Fecha Hora Latitud Longitud Profundidad ML


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REGISTRO UGSC:

2013 SIGNIFICANT EARTHQUAKES ARCHIVE

1. 6.65km ESE of Ciudad Tecun Uman, Guatemala2013-09-07 00:13:29 UTC67.0 km deep2. 6.577km SSW of Atka, Alaska2013-09-04 02:32:33 UTC39.9 km deep3. 6.5Izu Islands, Japan region2013-09-04 00:18:24 UTC407.0 km deep4. 6.5Kepulauan Barat Daya, Indonesia2013-09-01 11:52:32 UTC132.1 km deep5. 7.094km ESE of Adak, Alaska2013-08-30 16:25:02 UTC33.5 km deep6. 4.23km NE of Spanish Springs, Nevada2013-08-27 00:51:43 UTC13.9 km deep7. 6.213km NNW of San Marcos, Mexico2013-08-21 12:38:30 UTC20.0 km deep8. 6.529km SSE of Blenheim, New Zealand2013-08-16 02:31:07 UTC10.0 km deep9. 6.698km WSW of Mutis, Colombia2013-08-13 15:43:15 UTC12.0 km deep10.5.913km E of Chabu, China2013-07-21 23:45:56 UTC9.8 km deep

PRIMER REGISTRO:

6.65KM ESE OF CIUDAD TECUN UMAN, GUATEMALA2013-09-07 00:13:29 UTC67.0 KM DEEP

Tectonic Summary

The September 7, 2013 M 6.6 earthquake near the west coast of Guatemala in the Middle America

subduction zone occurred close to the interface between the Cocos and North America plates. The

depth and style of faulting of the earthquake indicates slip likely occurred on a very shallow, or

near-vertical thrust fault consistent with intraplate faulting within the subducting Cocos plate,

rather than on the overlying thrust interface. At the latitude of this event, the Cocos plate moves

towards the north-northeast with respect to the North American plate at a rate of approximately78 mm/yr.

The broad scale tectonics of the western and southwestern coast of Central America are

dominated by the northeastward subduction of the Cocos oceanic plate beneath the North

America plate. Thrust- and normal-type earthquakes are a common occurrence along this plate

boundary and the Guatemala region, with events occurring both within the subduction zone - on

the megathrust interface and within the subducting plate - and also in the overriding plate. Over

the past 40 years, 27 events of M 6.0 or greater have occurred within 300 km of the September

2013 event. Events of note in this region include earthquakes on November 2012 (M 7.4) offshore

of Guatemala, which caused around 40 fatalities; September 1993 (M 7.2) offshore of Chiapas,

Mexico, which killed one person; and December 1983 (M 7.0) offshore of Guatemala. Other early20th century earthquakes in the Guatemala region include the August 1942 M 7.9 event, which

caused around 40 fatalities, and the April 1902 M 7.5 earthquake, which killed more than 5000

people.
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SEGUNDO REGISTRO:

SEISMOTECTONICS OF ALASKA

The Aleutian arc extends approximately 3,000 km from the Gulf of Alaska in the east to the

Kamchatka 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 theAleutian 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 northwest at

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 the

Fox 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 the

west. 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 of convergence,

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 the

Commander 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 is located 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, predominantly strike-slip

events with magnitudes between M5-6. Deeper earthquakes do occur, albeit rather scarcely and

with small magnitudes (M


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TERCER:

SEISMOTECTONICS OF THE PHILIPPINE SEA AND VICINITY

The Philippine Sea plate is bordered by the larger Pacific and Eurasia plates and the smaller Sunda

plate. The Philippine Sea plate is unusual in that its borders are nearly all zones of plate

convergence. The Pacific plate is subducted into the mantle, south of Japan, beneath the Izu-Boninand Mariana island arcs, which extend more than 3,000 km along the eastern margin of the

Philippine Sea plate. This subduction zone is characterized by rapid plate convergence and high-

level seismicity extending to depths of over 600 km. In spite of this extensive zone of plate

convergence, the plate interface has been associated with few great (M>8.0) megathrust

earthquakes. This low seismic energy release is thought to result from weak coupling along the

plate interface (Scholz and Campos, 1995). These convergent plate margins are also associated

with unusual zones of back-arc extension (along with resulting seismic activity) that decouple the

volcanic island arcs from the remainder of the Philippine Sea Plate (Karig et al., 1978; Klaus et al.,

1992).

South of the Mariana arc, the Pacific plate is subducted beneath the Yap Islands along the Yaptrench. The long zone of Pacific plate subduction at the eastern margin of the Philippine Sea Plate

is responsible for the generation of the deep Izu-Bonin, Mariana, and Yap trenches as well as

parallel chains of islands and volcanoes, typical of circum-pacific island arcs. Similarly, the

northwestern margin of the Philippine Sea plate is subducting beneath the Eurasia plate along a

convergent zone, extending from southern Honshu to the northeastern coast of Taiwan,

manifested by the Ryukyu Islands and the Nansei-Shoto (Ryukyu) trench. The Ryukyu Subduction

Zone is associated with a similar zone of back-arc extension, the Okinawa Trough. At Taiwan, the

plate boundary is characterized by a zone of arc-continent collision, whereby the northern end of

the Luzon island arc is colliding with the buoyant crust of the Eurasia continental margin offshore

China.

Along its western margin, the Philippine Sea plate is associated with a zone of oblique

convergence with the Sunda Plate. This highly active convergent plate boundary extends along

both sides the Philippine Islands, from Luzon in the north to the Celebes Islands in the south. The

tectonic setting of the Philippines is unusual in several respects: it is characterized by opposite-

facing subduction systems on its east and west sides; the archipelago is cut by a major transform

fault, the Philippine Fault; and the arc complex itself is marked by active volcanism, faulting, and

high seismic activity. Subduction of the Philippine Sea Plate occurs at the eastern margin of the

archipelago along the Philippine Trench and its northern extension, the East Luzon Trough. The

East Luzon Trough is thought to be an unusual example of a subduction zone in the process of

formation, as the Philippine Trench system gradually extends northward (Hamburger et al., 1983).

On the west side of Luzon, the Sunda Plate subducts eastward along a series of trenches, including

the Manila Trench in the north, the smaller less well-developed Negros Trench in the central

Philippines, and the Sulu and Cotabato trenches in the south (Cardwell et al., 1980). At its northern

and southern terminations, subduction at the Manila Trench is interrupted by arc-continent

collision, between the northern Philippine arc and the Eurasian continental margin at Taiwan and

between the Sulu-Borneo Block and Luzon at the island of Mindoro. The Philippine fault, which

extends over 1,200 km within the Philippine arc, is seismically active. The fault has been associated


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CUARTO:

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 until it 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 of

approximately 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 interplate megathrust earthquake occurred 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.

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 of Australia-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 been recorded since 1900, including three shallow thrust fault M8.1 events in1906, 1919, and 2007.

The western end of the Australia-Pacific plate boundary is perhaps the most complex portion of this

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 convergent deformation. The dominant convergence is accommodated by


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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 2-8

mm/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 (


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QUINTO:

EVENT TIME ALASKA

1. 2013-08-30 16:25:02 UTC2. 2013-08-30 04:25:02 UTC-12:00 at epicenter3. 2013-08-30 11:25:02 UTC-05:00 system time

Location

51.610N 175.361W depth=33.5km (20.8mi)

The August 30, 2013 M 7.0 earthquake southeast of Adak, Alaska, occurred as the result of thrust faulting on

or near the subduction zone interface between the Pacific and North America plates. At the location of this

event, the Pacific plate moves towards the northwest with respect to North America at a rate of

approximately 73 mm/yr, beginning its descent into the mantle at the Aleutian trench approximately 130 km

south of the August 30 earthquake. The depth and mechanism of this earthquake are consistent with it

occurring along the megathrust interface between these two plates.

The Aleutians Arc is familiar with large earthquakes two-dozen events of M 6.5 or larger have occurred

over the last century within 250 km of the August 30 earthquake. The largest of these was an Mw 8.6

earthquake in March of 1957, whose hypocenter was located just 15 km south of the August 30 earthquake.

Aftershocks associated with the 1957 event extended for more than 1000 km along the arc, roughly from

the International Dateline in the west to Unimak Island in the east. The 1957 earthquake also resulted in a

large tsunami that was observed throughout the Pacific Basin, and caused damage locally along the Aleutian

Arc and in Hawaii. Other large nearby events include the May 1986 Mw 8.0 earthquake 40 km to the

southeast, and the June 1996 Mw 7.9 earthquake 150 km to the west. Neither of these more recent events

are known to have caused fatalities or significant damage.


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Registro de Aceleraciones 2013

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