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翻訳と辞書　辞書検索 [ 開発暫定版 ] スポンサード リンク Gutenberg–Richter law ： ウィキペディア英語版 Gutenberg–Richter law In seismology, the Gutenberg–Richter law〔Gutenberg and Richter, , pages 17–19 ("Frequency and energy of earthquakes").〕 (GR law) expresses the relationship between the magnitude and total number of earthquakes in any given region and time period of ''at least'' that magnitude. : $\backslash !\backslash ,\backslash log\_\; N\; =\; a\; -\; b\; M$ or : $\backslash !\backslash ,N\; =\; 10^$ Where: * $\backslash !\backslash ,\; N$ is the number of events having a magnitude $\backslash !\backslash ,\; \backslash ge\; M$ * $\backslash !\backslash ,\; a$ and $\backslash !\backslash ,\; b$ are constants == Background == The relationship between earthquake magnitude and frequency was first proposed by Charles Francis Richter and Beno Gutenberg in a paper published in 1956.〔(Gutenberg, B., Richter, C. F., 1956. Magnitude and Energy of Earthquakes. Annali di Geofisica, 9: 1–15 )〕 This power law relationship between event magnitude and frequency of occurrence is remarkably common, although the values of a and b may vary significantly from region to region or over time. The parameter b (commonly referred to as the "b-value") is commonly close to 1.0 in seismically active regions. This means that for given a frequency of 4.0 event there will be 10 times as many magnitude 3.0 quakes and 100 times as many magnitude 2.0 quakes. There is some variation of b-values in the approximate range of 0.5 to 2 depending on the source environment of the region.〔Bhattacharya ''et al'', p. 120〕 A notable example of this is during earthquake swarms when b can become as high as 2.5, thus indicating a very high proportion of small earthquakes to large ones. There is debate concerning the interpretation of some observed spatial and temporal variations of b-values. The most frequently cited factors to explain these variations are: the stress applied to the material,〔Scholz, C. H. (1968), the frequency-magnitude relation of microfracturing in rock and its relation to earthquakes, BSSA, 58(1), 399–415.〕 the depth,〔Mori, J., et R. E. Abercombie (1997), Depth dependence of earthquake frequency-magnitude distributions in California: Implication for rupture initiation, Journal of Geophysical Research, 102(B7), 15081–15090.〕 the focal mechanism,〔Schorlemmer, D., S. Wiemer, et M. Wyss (2005), Variations in earthquake-size distribution across different stress regimes, Nature, 437, 539–542, doi: 10.1038/nature04094.〕 the strength heterogeneity of the material,〔Mogi, K. (1962), Magnitude frequency relations for elastic shocks accompanying fractures of various materials and some related problems in earthquakes, Bull. Earthquake Res. Inst. Univ. Tokyo, 40, 831–853.〕 and the proximity of macro-failure. The ''b''-value decrease observed prior to the failure of samples deformed in the laboratory〔Lockner, D. A., et J. D. Byerlee (1991), Precursory AE patterns leading to rock fracture, in Vth Conf. AE/MS Geol. Str. and Mat., édité par Hardy, pp. 45–58, Trans Tech Publication, Germany, The pennsylvania State University.〕 has led to the suggestion that this is a precursor to major macro-failure.〔Smith, W. D. (1981), The ''b''-value as an earthquake precursor, Nature, 289, 136–139; doi:10.1038/289136a0.〕 Statistical physics provides a theoretical framework for explaining both the steadiness of the Gutenberg–Richter law for large catalogs and its evolution when the macro-failure is approached, but application to earthquake forecasting is currently out of reach.〔Amitrano, D. (2012), Variability in the power-law distributions of rupture events, how and why does b-value change, Eur. Phys. J.-Spec. Top., 205(1), 199–215, doi:10.1140/epjst/e2012-01571-9.〕 Alternatively, a b-value significantly different from 1.0 may suggest a problem with the data set; e.g. it is incomplete or contains errors in calculating magnitude. There is an apparent b-value decrease for smaller magnitude event ranges in all empirical catalogues of earthquakes. This effect is described as "roll-off" of the b-value, a description due to the plot of the logarithmic version of the GR law becoming flatter at the low magnitude end of the plot. This may in large part be caused by incompleteness of any data set due to the inability to detect and characterize small events. That is, many low-magnitude earthquakes are not catalogued because fewer stations detect and record them due to decreasing instrumental signal to noise levels. Some modern models of earthquake dynamics, however, predict a physical roll-off in the earthquake size distribution.〔Bhattacharya ''et al'', pp. 119–121 Pelletier, pp. 34–36.〕 The ''a-value'' is of less scientific interest and simply indicates the total seismicity rate of the region. This is more easily seen when the GR law is expressed in terms of the total number of events: :$N\; =\; N\_\backslash mathrm\; 10^\; \backslash$ :where :$N\_\backslash mathrm\; =\; 10^a,\; \backslash$ the total number of events. Modern attempts to understand the law involve theories of self-organized criticality or self similarity. 抄文引用元・出典: フリー百科事典『 ウィキペディア（Wikipedia）』 ■ウィキペディアで「Gutenberg–Richter law」の詳細全文を読む スポンサード リンク 翻訳と辞書 : 翻訳のためのインターネットリソース Copyright(C) kotoba.ne.jp 1997-2016. All Rights Reserved.