{"refrec":{"BRefID":230228,"RR":"<b>Okal, E.A.</b> (2013). From 3-Hz P waves to <sub>0</sub>S<sub>2</sub>: No evidence of a slow component to the source of the 2011 Tohoku earthquake. <i>Pure Appl. Geophys. 170(6-8)</i>: 963-973. <a href=\"http://dx.doi.org/10.1007/s00024-012-0500-x\" target=\"_blank\">http://dx.doi.org/10.1007/s00024-012-0500-x</a>","BEntID":221943,"PublicFlag":1,"CheckedFlag":1,"wosflag":1,"vabbflag":null,"RefStringPartII":". <i>Pure Appl. Geophys. 170(6-8)</i>: 963-973. <a href=\"http://dx.doi.org/10.1007/s00024-012-0500-x\" target=\"_blank\">http://dx.doi.org/10.1007/s00024-012-0500-x</a>","DocTypID":8,"DocType":"Journal article","MarineFlag":1,"FreshFlag":0,"BrackishFlag":0,"TerrestrialFlag":0,"Authorstring":"Okal, E.A.","OrigTitleTranslFlag":0,"Authorstringtrunc":"Okal, E.A.","Englishabstract":"In the hours following the 2011 Honshu event, and as part of tsunami warning procedures at the<span class=\"a-plus-plus emphasis\"> Laboratoire de Géophysique</span> in Papeete, Tahiti, the seismic source of the event was analyzed using a number of real-time procedures. The ultra-long period mantle magnitude algorithm suggests a static moment of 4.1 × 10<sup class=\"a-plus-plus\">29</sup> dyn cm, not significantly different from the National Earthquake Information Center (NEIC) value obtained by <em class=\"a-plus-plus\">W</em>-phase inversion. The slowness parameter, <span class=\"a-plus-plus inline-equation id-i-eq4\">  <span class=\"a-plus-plus equation-source format-t-e-x\">$\\Uptheta = -5.65, $</span> </span> is slightly deficient, but characteristic of other large subduction events such as Nias (2005) or Peru (2001); it remains significantly larger than for slow earthquakes such as Sumatra (2004) or Mentawai (2010). Similarly, the duration of high-frequency (2–4 Hz) <em class=\"a-plus-plus\">P</em> waves in relation to seismic moment or estimated energy, fails to document any slowness in the seismic source. These results were confirmed in the ensuing weeks by the analysis of the lowest-frequency spheroidal modes of the Earth. A dataset of 117 fits for eight modes (including the gravest one, <sub class=\"a-plus-plus\">0</sub> <em class=\"a-plus-plus\">S</em> <sub class=\"a-plus-plus\">2</sub>, and the breathing mode, <sub class=\"a-plus-plus\">0</sub> <em class=\"a-plus-plus\">S</em> <sub class=\"a-plus-plus\">0</sub>) yields a remarkably flat spectrum, with an average moment of 3.5 × 10<sup class=\"a-plus-plus\">29</sup> dyn cm (*/1.07). This behavior of the Tohoku earthquake explains the generally successful real-time modeling of its teleseismic tsunami, based on available seismic source scaling laws. On the other hand, it confirms the dichotomy, among mega-quakes (<em class=\"a-plus-plus\">M</em> <sub class=\"a-plus-plus\">0</sub> &gt; 10<sup class=\"a-plus-plus\">29</sup> dyn cm) between regular events (Nias, 2005; Chile, 2010; Sendai, 2011) and slow ones (Chile, 1960; Alaska, 1964; Sumatra, 2004; and probably Rat Island, 1965), whose origin remains unexplained.","AbstractOtherLang":null,"BibLvlCode":"AS","StandardTitle":"From 3-Hz P waves to <sub>0</sub>S<sub>2</sub>: No evidence of a slow component to the source of the 2011 Tohoku earthquake","OrigTitleLangCode":"en","OrigTitleLangCodeExtended":"eng","OrigTitleLangID":15,"DateLastModified":{"date":"2026-06-11 01:31:50.114136","timezone_type":1,"timezone":"+02:00"},"UserAccessRight":null,"UserAccID":null,"AuthorKeywords":"Tohoku earthquake; Slow components; Seismological quantification; Mega earthquakes ","OtherDescriptors":null,"Notes":null,"AnaPub":2013,"MonPub":null,"DateUpdate":"2018-02-13","DateCreate":"2013-10-24","SecASFANote":null,"ConfID":null,"PeerRev":1,"VlizCoreFlag":1,"WoScode":"WOS:000320044100002","VABBcode":null,"OpenAcc":0,"DOI":"10.1007/s00024-012-0500-x"},"refs":null,"anarec":{"AnaID":230228,"PubliDate":2013,"Pagination":"963-973","XtraPublOfAnaID":null,"ISBN":null,"Volume":"170","Issue":"6-8","BRefMon":null,"BRefMonRR":null,"BRefXtra":null,"BRefXtraRR":null,"SerBRefID":43723,"SerRR":"Pure and Applied Geophysics. 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