Field occurrences of liquefaction-induced features: a primer for engineering geologic analysis of paleoseismic shaking

Obermeier, Stephen F.; Olson, Scott M.; Green, Russell A.

doi:10.1016/j.enggeo.2004.07.009

Cited by 139 publications

(65 citation statements)

References 33 publications

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“…2) are not reported, liquefied and intruded gravels score high on their list. This observation is in agreement with Obermeier (1996) and Obermeier et al (2005), who state that the threshold magnitude to induce liquefaction in the most susceptible gravel is around M = 7 to 7AE5. Because this location is only 3 km from the northern major Alpujarras fault zone (Fig.…”

Section: Frequency and Magnitude Of Palaeoseismic Events Based On Sedsupporting

confidence: 81%

“…In sandy sediments, the minimum earthquake magnitude to form liquefaction features is about moment magnitude M = 5AE5 (Obermeier, 1996), but they become common in case of magnitudes above 6AE6 (Ambraseys, 1988;Obermeier et al, 2005). Most liquefaction and flowage features occur within 15 km wide zones along observed tectonic structures (Kanaori et al, 1993), and empirical relationships between both earthquake intensity and magnitude and the area over which liquefaction takes place for historical earthquakes in Italy have been established by Galli (2000).…”

Section: Introductionmentioning

confidence: 99%

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Evidence for Late Messinian seismites, Nijar Basin, south‐east Spain

Fortuin¹,

Dabrio

2008

Sedimentology

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The Feos Formation of the Nijar Basin comprises sediments deposited during the final stage of the Messinian salinity crisis when the Mediterranean was almost totally isolated. Levels of soft-sediment deformation structures occur in both conglomeratic alluvial sediments deposited close to faults and the hyposaline Lago Mare facies, a laminated and thin-bedded succession of whitish chalky marls and intercalated sands alternating with non-marine coastal plain deposits. Deformation structures in the coarse clastics include funnel-shaped depressions filled with conglomerate, liquefaction dykes terminating downwards in gravel pockets, soft-sediment mixing bodies, chaotic intervals and flame structures. Evidence for soft-sediment deformation in the fine-grained Lago Mare facies comprises syndepositional faulting and fault-grading, sandstone dykes, mixed layers, slumping and sliding of sandstone beds, convolute bedding, and pillar and flame structures. The soft-sediment deformed intervals resemble those ascribed elsewhere to seismic shaking. Moreover, the study area provides the appropriate conditions for the preservation of deformation structures induced by seismicity; such as location in a tectonically active area, variable sediment input to produce heterolithic deposits and an absence of bioturbation. The vertical distribution of soft-sediment deformation implies frequent seismic shocks, underlining the importance of seismicity in the Betic region during the Late Messinian when the Nijar Basin became separated from the Sorbas Basin to the north. The presence of liquefied gravel injections in the marginal facies indicates strong earthquakes (M ‡ 7). The identification of at least four separate fissured levels within a single Lago Mare interval suggests a recurrence interval for large magnitude earthquakes of the order of millennia, assuming that the cyclicity of the alternating Lago Mare and continental intervals was precession-controlled. This suggestion is consistent with the present-day seismic activity in SE Spain.

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Section: Frequency and Magnitude Of Palaeoseismic Events Based On Sedsupporting

confidence: 81%

Section: Introductionmentioning

confidence: 99%

Evidence for Late Messinian seismites, Nijar Basin, south‐east Spain

Fortuin¹,

Dabrio

2008

Sedimentology

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“…The first phase entails the performance of field investigations, wherein paleoliquefaction features are located, mapped, and dated. The reader is referred to Obermeier et al (2001Obermeier et al ( , 2005 for broad overviews of paleoliquefaction field investigation, and to the intensive investigations by Obermeier and Dickenson (2000), Tuttle (2001), Talwani and Schaeffer (2001), Cox et al (2004), and Tuttle et al (2002aTuttle et al ( , 2002bTuttle et al ( , 2005 for specific case studies. The second phase, and the focus of this study, is back-analysis, wherein quantitative techniques are used to determine the magnitude of the causative paleoearthquake and better constrain its source location.…”

Section: Introductionmentioning

confidence: 99%

Development of magnitude-bound relations for paleoliquefaction analyses: New Zealand case study

Maurer

Green

Quigley

et al. 2015

Engineering Geology

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a b s t r a c tMagnitude-bound relations are often used to estimate paleoearthquake magnitudes from paleoliquefaction data. This study proposes New Zealand-based magnitude-bound curves that are developed using (a) liquefaction field observations and (b) a newly proposed back-calculation approach that combines the simplified liquefaction evaluation procedure with a regionally appropriate ground motion prediction equation. For (b) both deterministic and probabilistic frameworks are proposed. The magnitude bound curves back-calculated using either the deterministic or probabilistic frameworks are advantageous in that they can be used to predict the spatial distribution of liquefaction in regions where historical liquefaction field observations are limited or poorly documented, and because soil-and site-specific conditions can be incorporated into magnitude-bound analyses. Moreover, curves developed using the probabilistic framework allow for the range of possible causative earthquake magnitudes to be better understood and quantified. To demonstrate the use of the proposed relations, paleoliquefaction features discovered in eastern Christchurch (NZ) are analyzed. The 1869~M w 4.8 Christchurch earthquake and/or 1717~M w 8.1 Alpine Fault earthquake are found to be the most likely candidates amongst known historical and paleoearthquakes for triggering liquefaction over the permissible time range (ca. 1660 to 1905 A.D.). This study demonstrates the potential of the proposed magnitude-bound curves to provide insight in to past, present, and future hazards, proving their utility even in cases of limited evidence. The approach of developing and applying magnitude bound curves proposed herein is not limited to parts of New Zealand, but rather, can be applied worldwide.

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“…The large well documented seism (the so called Lisbon earthquake -1755) had an estimated magnitude of 8.5 -9.0 (Gutscher et al, 2006). According to several authors, Obermeier et al (2005) refers that the minimum earthquake magnitude to form liquefaction features is about moment magnitude M 5.5, a value widely exceeded by the 1755 earthquake.…”

Section: Final Remarksmentioning

confidence: 99%

“…The disturbance inside layer 2 seemed to be related to liquefaction (considered by Olson et al (2005) and Obermeier et al (2005), as a transformation of a saturated granular material from a solid to a liquefied state, which might be induced by seismic shaking) and fluidization. Nikolaeva (2009) summarizes the following main criteria for liquefaction and fluidization: (i) "composition of sediments prone to plasticity, liquefaction, and fluidization; (ii) absence of detectable effects of slope instability; (iii) independence of deformation structures of sediment stacking patterns; (iv) stratigraphic position of deformation units between undeformed sediments; (v) cyclic repetition of structures in the section as evidence for recurrence of the causative events; (vi) similarity to structures proven to result from seismic shaking; (vii) proximity to an active seismic zone and (viii) proximity to faults which have been active through the Cenozoic".…”

Section: Final Remarksmentioning

confidence: 99%