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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