afford的过去式
\documentclass{article}
\upackage{graphicx}
\upackage[round]{natbib}
\bibliographystyle{plainnat}
\upackage[pdfstartview=FitH,%
bookmarksnumbered=true,bookmarksopen=true,%
colorlinks=true,pdfborder=001,citecolor=blue,%
linkcolor=blue,urlcolor=blue]{hyperref}
\begin{document}
\title{Rearch plan under the Post-doctorate program at xx University}
%\subtitle{aa}
\author{Robert He}
\date{2008/04/23}
\maketitle
\ction{Rearch Title}
~~~~Crustal ismic anisotropy in the xx using Moho P-to-S converted phas.
\ction{Rearch Background \& Purpos}
~~~~Shear-wave splitting analys provide us a new way to study the ismic structure and mantle dynamics in the crust and mantle. The crustal anisotropy is developed due to various reasons including lattice-preferred orientation (LPO) of mineral crystals and oriented cracks.
\newline
Traditionally, the earthquakes occurring in the curst and the subducting plates are lected to determine the ismic anisotropy of the crust. However, none of the methods can help us to ass
s the anisotropy in the whole crust. Becau crustal earthquakes mostly are located in the upper crust, they do not provide information of lower crust. On the other hand, earthquakes in the subducting plates provide information of the whole crust but combined with upper mantle. However, it’s difficult to extract the sole contribution of the crust from the measurement. Fortunately P-to-S converted waves (Ps) at the Moho are ideal for investigation of crustal ismic anisotropy since they are influenced only by the medium above the Moho. Moho. Figure \ref{crustalspliting}~schematically shows the effects of shear wave splitting on Moho Ps phas. Initially, a near-vertically incident P wave generates a radially polarized converted shear wave at the crust-mantle boundary. The phas, polarized into fast and slow directions, progressively split in time as they propagate through the anisotropic media. Here, the Ps waves can be obtained from teleismic receiver function analysis.
%
%
\begin{figure}[htbp]
\begin{center}
\includegraphics[width=0.47\textwidth]{crustalsplit.png}
\caption{The effects of shear wave splitting in the Moho P to S converted pha. Top shows a schematic ismogram in the fast/slow coordinate system with split horizontal Ps components.(cited from: McNamara and Owens, 1993)}
\label{crustalspliting}
\end{center}
\end{figure}
郑州美甲%
%
The Korean Peninsula is compod of three major Precambrian massifs, the Nangrim, Gyeongii, and Yeongnam massifs(Fig.\ref{geomap}). The Pyeongbuk-Gaema Massif forms the southern part of Liao-Gaema Massif of southern Manchuria, and the Gyeonggi and Mt. Sobaeksan massifs of the peninsula are correlated with the Shandong and Fujian Massifs of China.
%
\begin{figure}[htbp]
\begin{center}
\includegraphics[width=0.755\textwidth]{geo.png}
\caption{Simplified geologic map. NCB: North China block; SCB: South China block.(cited from: Choi et al., 2006)}
英语学习辅导报官网\label{geomap}
\end{center}
\end{figure}
liuhecai%
Our purpo of the study is to measure the shear wave splitting parameters in the crust of the Korean Peninsula. The shear wave splitting parameters include the splitting time of shear energy
between the fast and slow directions, as well as fast-axis azimuthal direction in the Korean Peninsula. The two parameters provide us constraints on the mechanism causing the crustal anisotropy. From the splitting time, the layer thickness of anisotropy will be estimated. Whether crustal anisotropy mainly contributed by upper or lower crustal or both will be determined. Bad on the fast-axis azimuthal direction, the tectonic relation between northeastern China and the Korean peninsula will be discusd.
\ction{Rearch Methods}
~~~~Several methods have been introduced for calculation of receiver functions. An iterative deconvolution technique may be uful for this study since it produces more stable receiver function results than others. The foundation of the iterative deconvolution approach is a least-squares minimization of the difference between the obrved horizontal ismogram and a predicted signal generated by the convolution of an iteratively updated spike train with the vertical-component ismogram. First, the vertical component is cross-correlated with the radial component to estimate the lag of the first and largest spike in the receiver function (the optimal time is that of the largest peak in the absolute n in the cross-correlation signal). Then the convolution of the current estimate of the receiver function with the vertical-component ismogram is subtracted from the radi
al-component ismogram, and the procedure is repeated to estimate other spike lags and amplitudes. With each additional spike in the receiver function, the misfit between the vertical and receiver-function convolution and the radial component ismogram is reduced, and the iteration halts when the reduction in misfit with additional spikes becomes insignificant.
\newline
For all measurement methods of shear-wave splitting, time window of waveform should be lected. Conventionally the shear-wave analysis window is picked manually. However, manual window lection is laborious and also very subjective; in many cas different windows give very different results.
珠海翻译\newline
In our study, the automated S-wave splitting technique will be ud, which improves the quality of shear-wave splitting measurement and removes the subjectivity in window lection. First, the splitting analysis is performed for a range of window lengths. Then a cluster analysis is applied in order to find the window range in which the measurements are stable. Once clusters of stable results are found, the measurement with the lowest error in the cluster with the lowest variance is prented
for the analysis result.
\ction{Expected results \& their contributions}
~~~~First, the teleismic receiver functions(RFs) of all stations including radial and transver RFs can be gained. Bad on the analysis of RFs, the crustal thickness can be estimated in the Korean Peninsula. Then most of the expected results are the shear-wave splitting parameters from RFs analysis in the crust beneath the Korean Peninsula. The thickness of anisotropic layer will be estimated in the region when the obrved anisotropy is assumed from a layer of lower crustal material.All the results will help us to understand the crustal anisotropy source.
\newline
cidrCrustal anisotropy can be interpreted as an indicator of the crustal stress/strain regime. In addition, since SKS splitting can offer the anisotropy information contributed by the upper mantle but combined with the crust, the sole anisotropy of the upper mantle can be attracted from the measurement of SKS splitting bad on the crustal splitting result.
%\cite{frogge2007}
%%
%\citep{frogge2008}
%%
vegetable%\citep{s-frogge2007}修葺
% 5. References
中秋晚会致辞\begin{thebibliography}{99}
\item Burdick, L. J. and C. A. Langston, 1977, Modeling crustal structure through the u of converted phas in teleismic body waveforms, \textit{Bull. Seismol. Soc. Am.}, 67:677-691.
ets\item Cho, H-M. et al., 2006, Crustal velocity structure across the southern Korean Peninsula from ismic refraction survey, \textit{Geophy. Res. Lett.} 33,
doi:10.1029/2005GL025145.
\item Cho, K. H. et al., 2007, Imaging the upper crust of the Korean peninsula by surface-wave tomo
graphy, \textit{Bull. Seismol. Soc. Am.}, 97:198-207.
\item Choi, S. et al., 2006, Tectonic relation between northeastern China and the Korean peninsula revealed by interpretation of GRACE satellite gravity data,
\textit{Gondwana Rearch}, 9:62-67.
\item Chough, S. K. et al., 2000, Tectonic and dimentary evolution of the Korean peninsula: a review and new view, \textit{Earth-Science Reviews}, 52:175-235.
\item Crampin, S., 1981, A review of wave motion in anisotropic and cracked elastic-medium, \textit{Wave Motion}, 3:343-391.
\item Fouch, M. J. and S. Rondenay, 2006, Seismic anisotropy beneath stable continental interiors, \textit{Phys. Earth Planet. Int.}, 158:292-320.
\item Herquel, G. et al., 1995, Anisotropy and crustal thickness of Northern-Tibet. New constraints for tectonic modeling, \textit{Geophys. Res. Lett.}, 22(14):1 925-1 928.
\item Iidaka, T. and F. Niu, 2001, Mantle and crust anisotropy in the eastern China region inferred from waveform splitting of SKS and PpSms, \textit{Earth Planets Space}, 53:159-168.
