The 1968 Inangahua, New Zealand, and 1994 Northridge, California, earthquakes: Implications for northwest Nelson

Yeats, Robert S.

doi:10.1080/00288306.2000.9514911

Cited by 9 publications

(3 citation statements)

References 33 publications

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“…Bedding-plane faults have ruptured coseismically and produced surface scarps in conjunction with large earthquakes on deeper structures (Lensen and Otway, 1971;Philip and Meghraoui, 1983;Hull, 1990;Treiman, 1995;Yeats, 2000). While in some cases bedding-plane faults above thrust wedges and passive roof duplexes root in thrust ramps or roof thrusts (Banks and Warburton, 1986;Guzofski et al, 2007), in other cases bedding-plane reverse faults root in the axial plane region of folds (Shaw and Suppe, 1994;Ishiyama et al, 2004).…”

Section: Can Bedding-plane Faults Generate Earthquakes?mentioning

confidence: 96%

Earthquakes generated from bedding plane-parallel reverse faults above an active wedge thrust, Seattle fault zone

Kelsey

Sherrod

Nelson

et al. 2008

Geological Society of America Bulletin

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A key question in earthquake hazard analysis is whether individual faults within fault zones represent independent seismic sources. For the Seattle fault zone, an upper plate structure within the Cascadia convergent margin, evaluating seismic hazard requires understanding how north-side-up, bedding-plane reverse faults, which generate late Holocene fault scarps, interact with the north-vergent master-ramp thrust and overlying backthrust of the fault zone. A regional uplift at A.D. 900-930 involved an earthquake that nucleated at depth and included slip on both the master-ramp thrust and the backthrust. This earthquake also included slip on some of the <6-km-deep north-side-up, bedding-plane reverse faults. At locales where the north-side-up reverse faults intersect the Puget Sound coast, an earthquake a few centuries earlier than the A.D. 900-930 regional uplift only uplifted areas within hundreds of meters north of the reverse faults. We infer that the bedding-plane reverse faults are seismogenic because shore platforms near the reverse faults have been abruptly uplifted during earthquakes when other shorelines in the Seattle fault zone were unaffected. Faults of the Seattle fault zone therefore can both produce regional uplift earthquakes, with or without surface displacement on the reverse faults, and produce earthquakes that rupture the bedding-plane reverse faults causing fault scarps and uplift localized to hundreds of meters north of these faults. This latter type of earthquake has occurred at least twice and perhaps three times in the late Holocene, and all these earthquakes preceded the regional coseismic uplift of A.D. 900-930. To account for the paleoseismic observations, we propose that the Seattle fault zone is a wedge thrust, with the leading edge being a fault-bend, wedge thrust fold. The active axial surface of the wedge thrust fold is pinned at the tip of the wedge, and a steeply north-dipping sequence of Tertiary sediment forms the south limb of the wedge thrust fold. Some of these steeply north-dipping, bedding-plane surfaces are seismogenic reverse faults that produce scarps. Earthquakes on the wedge thrust produce the regional coseismic uplift events, and earthquakes within the faultbend fold cause the local uplift earthquakes. Thus, bedding-plane faults can rupture during earthquakes when the wedge thrust does not rupture but instead continues to accumulate seismic energy.

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Section: Can Bedding-plane Faults Generate Earthquakes?mentioning

confidence: 96%

Earthquakes generated from bedding plane-parallel reverse faults above an active wedge thrust, Seattle fault zone

Kelsey

Sherrod

Nelson

et al. 2008

Geological Society of America Bulletin

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“…The best candidates might be Japan, Turkey, China, New Zealand, and Iran, all regions where much is already known about the distribution of active faults and fault networks, and more is being learned from paleoseismic studies. In New Zealand, for example, the Alpine plate-boundary fault appears to be quiet for the moment, except for the strike-slip faults of Marlborough, but the Range-and-Basin Province of northwestern South Island, with low long-term slip rates, was struck by large earthquakes in 1929and 1968, and smaller ones in 1962and 1991(Anderson et al, 1993Yeats, 2000). Parts of the Sierras Pampeanas in northwest Argentina, with earthquakes in 1893, 1944, 1952, and 1977, exhibit a seismic moment rate an order of magnitude higher than predicted by the geology (T. Rockwell, 2007, personal commun.…”

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confidence: 97%

Paleoseismology: Why can't earthquakes keep on schedule?

Yeats

2007

Geol

Self Cite

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“…Although Yeats et al (1981) suggested that faults parallel to bedding may generate earthquakes without an external trigger mechanism from adjacent, deeper faults (review in Kelsey et al (2008)), geological evidence from other tectonically active regions suggests that flexural-slip faults may be activated co-seismically during rupture of linked, deeper-seated crustal structures (e.g., Hull, 1990;Treiman, 1995;Yeats, 2000). For example, the 1981 Mw 2.5 Lompac earthquake of California, U.S. (Yerkes et al, 1983), the 1980 Mw 7.3 El Asnam earthquake in Algeria (Philip & Meghraoui, 1983), the Mw 6.6 2008 Nura earthquake in Kyrgyzstan (Patyniak, 2022;Patyniak et al, 2021), and the Mw 7.0 1944 San Juan earthquake in Argentina (Rockwell et al, 2014) may belong to this group of seismogenic faults.…”

Section: Seismogenic Potential Of Faults In the Santa Bárbara Systemmentioning

confidence: 99%

Kinematic Evolution of the Santa Bárbara System in the Foreland of the Central Andes of Northwestern Argentina (26°S)

Arnous,

García,

Pingel

et al. 2024

Tectonics

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Compared to the thin‐skinned Subandean foreland fold‐and‐thrust belt of northern Argentina and Bolivia, the tectonically active morphotectonic province of the Santa Bárbara System in the Andean broken foreland of northwestern Argentina is characterized by a temporally and spatially disparate deformation style. Although there is no well‐defined orogenic deformation front associated with the uplift of these basement‐cored, reverse‐fault bounded mountain ranges, there has been an overall eastward trend in Andean compressional deformation since the Miocene. While reactivation of basement anisotropies, such as early Paleozoic metamorphic fabrics and Cretaceous normal faults, has been proposed to have profoundly affected deformation processes in the Santa Bárbara System, other mechanisms involving Mesozoic and Cenozoic cover rocks may also have played an important role in orogenic deformation in this sector of the Andean foreland. We present structural field observations, interpretations of seismic reflection profiles, and kinematic modeling from the basins bordering the Candelaria Range in the southern sector of the Santa Bárbara System at 26°S. Our analysis features a 110‐km‐long structural cross section that images and links deep‐seated structures with shallow neotectonic faults. We find that regional shortening has been facilitated by several faults associated with a regional detachment at a depth of 23 km, resulting in total horizontal shortening of about 17% (18.4 km). While the deep‐seated first‐order structures seem closely linked to seismogenic processes in the Andean foreland, shallow second‐order structures within the sedimentary cover modify the intermontane landscapes and appear to be associated with aseismic creep.

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The 1968 Inangahua, New Zealand, and 1994 Northridge, California, earthquakes: Implications for northwest Nelson

Abstract: The 1968 Inangahua earthquake ruptured a westdipping, largely blind reverse fault, here called the Rotokohu

Cited by 9 publications

References 33 publications

Earthquakes generated from bedding plane-parallel reverse faults above an active wedge thrust, Seattle fault zone

Earthquakes generated from bedding plane-parallel reverse faults above an active wedge thrust, Seattle fault zone

Paleoseismology: Why can't earthquakes keep on schedule?

Kinematic Evolution of the Santa Bárbara System in the Foreland of the Central Andes of Northwestern Argentina (26°S)

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