Hainzl earthquake model

The earthquake model incorporates 3‐D elastic stress interactions and pore pressure variations due to fluid intrusion

fluids in rockseismic modellingseismic stress



Initial contribute: 2019-06-24


Institute of Geosciences, University of Potsdam, Potsdam, Germany
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Application-focused categoriesNatural-perspectiveSolid-earth regions

Detailed Description

Chinese {{currentDetailLanguage}} Chinese

Quoted from: Sebastian Hainzl, 2004. Seismicity patterns of earthquake swarms due to fluid intrusion and stress triggering. Geophysical Journal International. https://doi.org/10.1111/j.1365-246X.2004.02463.x

The analysed model is mostly similar to the model of Yamashita (1997, 1998), which was introduced to simulate seismicity patterns initiated by fluid migration in a narrow, porous, planar fault zone pre‐stressed by tectonic plate movement or local deformation and embedded in a 3‐D elastic half‐space. Additionally, we assume post‐seismic creep on the fracture zone which leads to realistic aftershock activity according to the Omori law. This new mechanism will be described in more detail in Section 2.1.

The model is adapted to the Vogtland earthquake swarm which occurred between August and December in the year 2000 in the Novy Kostel focal area. It is the most recent and best‐documented strong earthquake swarm in Vogtland/northwest Bohemia (Fig. 1a). The earthquake catalogue of this swarm was recorded by the WEBNET local seismic network (Horalek et al. 2000) and consists of more than 8400 earthquakes with local magnitude L≥−0.5 (Fischer 2003). The catalogue is found to be complete for the = 4823 earthquakes with L≥ 0.2 (Hainzl & Fischer 2002). Fig. 1(b) shows the earthquakes of this swarm event as a function of their occurrence times.

Figure 1

(a) The fault structure (line segments) of the Vogtland/northwest Bohemia earthquake swarm region and earthquake epicentres (circles). The main swarm area is marked by the ellipse enclosing the year 2000 swarm activity. (b) The local earthquake magnitudes of this swarm are shown as a function of time elapsed since 2000 August 28.

The fault plane of the Vogtland earthquake swarm is modelled with a 3 km × 3 km rectangular patch dipping 73°. The lower edge of the brittle segment is set to a depth of 10 km (see Fig. 2a). The fault is discretized into 50 × 50 cells of dimension 60 m × 60 m each. Earthquake slip occurs when the Coulomb failure stress (CFS) becomes positive at one cell, i.e. the Coulomb failure criterion is fulfilled (Harris 1998):
Here τ defines the shear and σ the normal stress (positive for compression), is the pore pressure and μ is the coefficient of friction. Earthquake slip on the fault affects neither the normal stress nor the mean stress on the fault plane. Thus, slip has no effect on the pore pressure if material properties (e.g. permeability) are constant. In contrast, fluid flow generally influences not only the pore pressure but also the stress field. However, because of the numerical costs that would be involved in modelling the full coupling, it is assumed here that the stress field is, to a first order, not influenced by fluid flow (pore pressure changes).
Figure 2

Illustration of the model configuration (a) and the assumed healing and slip characteristics (b).

The characteristics of co‐seismic slip are governed by a static/kinetic friction law (Ben‐Zion & Rice 1993). If sliding is initiated, the coefficient of friction μ, i.e. the frictional resistance, drops from its static value μ0 to its lower dynamic value μd and remains there until the earthquake is terminated. The dynamic weakening of the fault strength is accompanied by a drop in stress. The shear stress τ drops to the arrest stress τa which is smaller than the frictional dynamic stress μd(σ−) because of dynamic overshoot.

The stress change on the fault plane due to relative slip of one segment is calculated with the analytical solution given by Okada (1992) for an elastic Poisson solid with a rigidity of 30 GPa. For simplification, we assume the slip to always be in the strike direction, although this is not in perfect agreement with the observed Vogtland swarm where both normal and strike‐slip events occurred (Fischer 2003). However, the main characteristics of the model are expected to be independent of this restriction because the stress pattern on the fault changes only slightly for rotating slip on the same fault plane. In particular, the stress decreases inside the rupture zone in the same way, and increases everywhere else. This increase is only slightly larger in the direction of slip.

The sliding of one cell can lead to an instability in other cells, and so on. An earthquake ends when all cells are stable with regard to the Coulomb failure criterion (eq. 1). The duration of earthquakes is much shorter than the typical time separating subsequent earthquakes. Thus we assume instantaneous co‐seismic slip, or, in other words, that the whole earthquake occurs at the same time.

--According to "Seismicity patterns of earthquake swarms due to fluid intrusion and stress triggering"



Sebastian Hainzl (2019). Hainzl earthquake model, Model Item, OpenGMS, https://geomodeling.njnu.edu.cn/modelItem/ae7bd86e-7288-43af-8948-a9347c85d963


Initial contribute : 2019-06-24



Institute of Geosciences, University of Potsdam, Potsdam, Germany
Is authorship not correct? Feed back

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