Английская Википедия:Ibagué Fault
Шаблон:Short description Шаблон:Infobox fault The Ibagué Fault (Шаблон:Lang-es) is a major dextral slightly oblique strike-slip fault in the department of Tolima in central Colombia. The fault has a total length of Шаблон:Convert and runs along an average east-northeast to west-southwest strike of 067.9 ± 11 cross-cutting the Central Ranges of the Colombian Andes.
The fault is part of a regional shear zone and has been active in historical times, possibly associated with the 1825 Ibagué earthquake and an earthquake in 1942.
Etymology
The fault is named after Ibagué, the capital of Tolima.[1]
Description
Шаблон:Location map+ The Ibagué Fault crosses the central part and eastern slope of the Central Ranges of the Colombian Andes, close to the city of Ibagué. The fault strikes west-southwest to east-northeast, controlling the course of the Cocora River. The fault has a well developed fault trace with prominent linear fault ridges (whale backs) as much as Шаблон:Convert long and Шаблон:Convert high, fault scarplets aligned with ridges, sag ponds, fault-controlled drainage, tilted deposits and upwarping. There is about Шаблон:Convert of (young) displacement along strike as calculated from a "whale back" offset by the fault.[2] The fault, forming a series of ramps,[3] terminates at the Magdalena River, north of Guataquí.[4]
Tectonic framework
The Ibagué Fault forms part with the Garrapatas and Cucuana Faults a shear zone between the latitudes 4 and 5 degrees north. To the north of this zone, regional structures are oriented along a north-northeast strike, characterised by sinistral displacement, among others the San Jerónimo, Silvia-Pijao, Cauca-Almaguer, Murindó, Bituima-La Salina and Bucaramanga-Santa Marta Faults. The movement along these structures generates a transpressive tectonic regime, related to the collision of the Chocó Block in the west of Colombia, during the Late Miocene. To the south of the structural zone the Ibagué Fault belongs to, north-northeast striking faults are mostly dextral, such as the Buesaco-Aranda, Cali-Patía and Algeciras Faults. Those are produced by the oblique subduction of the Malpelo Plate, formerly considered belonging to the Nazca Plate with the continental margin of the South American Plate.[5]
The Ibagué Fault cross-cuts the central part of the Central Ranges and extends along a strike of approximately 070 to the east to the Middle Magdalena Valley. Along its trace it principally cuts Paleozoic metamorphic rocks of the Cajamarca Complex, the Jurassic age Ibagué Batholith consisting of granodiorites, tonalites, granites, porphyrics of andesitic and dacitic composition and extrusive rocks as pyroclastic deposits and lava,[6] Paleogene and Neogene sedimentary rocks of the Gualanday and Honda Groups and displacing and deforming the Neogene to Quaternary Ibagué Fan (Шаблон:Lang-es), which is of volcano-sedimentary origin.[2][7] The fault passes southeast of the Nevado del Ruiz and Cerro Machín volcanoes.[8][9]
Activity
A rate of Шаблон:Convert per year is estimated and Шаблон:Convert per year published,[10] based on deformed and offset Quaternary features and dated deposits. A calculated moment magnitude of 7.0-7.2 is based on most probable fault rupture length of about Шаблон:Convert, from Ibagué to Piedras.[2] The most recent movement is estimated at 1040 to 1280 AD on the basis of radiocarbon dated deposits.[11] Two epicentres of historical earthquakes are located close to the fault, an earthquake of May 22, 1942 with magnitude 5.8 and an intensity in Ibagué of VIII and the intensity VI 1825 Ibagué earthquake of January 1, 1825.[12]
See also
References
Bibliography
Maps
Further reading
- ↑ Diederix et al., 2006, p.492
- ↑ 2,0 2,1 2,2 Paris et al., 2000, p.50
- ↑ Cuéllar Cárdenas, 2014, p.43
- ↑ Plancha 245, 1999
- ↑ Montes et al., 2004, p.14
- ↑ Cuéllar Cárdenas et al., 2014, p.39
- ↑ Montes et al., 2004, p.15
- ↑ Montes et al., 2004, p.16
- ↑ Montes et al., 2004, p.17
- ↑ Diederix et al., 2006, p.502
- ↑ Montes et al., 2004, p.167
- ↑ Montes et al., 2004, p.18
