carltape at geodynamics.org carltape at geodynamics.org
Thu Mar 19 22:04:48 PDT 2009

Author: carltape
Date: 2009-03-19 22:04:47 -0700 (Thu, 19 Mar 2009)
New Revision: 14401

Modified:
Log:
Changes 6-40s to 6-30s in the flexwin paper and the manual_tuning.tex.

===================================================================
--- seismo/3D/ADJOINT_TOMO/flexwin_paper/latex/appendix.tex	2009-03-20 02:15:15 UTC (rev 14400)
+++ seismo/3D/ADJOINT_TOMO/flexwin_paper/latex/appendix.tex	2009-03-20 05:04:47 UTC (rev 14401)
@@ -165,7 +165,7 @@

%CHT modified

-For the \trange{6}{40} and \trange{3}{40} data, we use constant values of $r_0(t)=r_0$, $\mathrm{CC}_0(t)=\mathrm{CC}_0$, $\Delta\tau_0(t)=\Delta\tau_0$, and $\Delta \ln A_0(t)=\Delta \ln A_0$. We exclude any arrivals before the $P$ wave and after the Rayleigh wave. This is achieved by the box-car function for $w_E(t)$:
+For the \trange{6}{30} and \trange{3}{30} data, we use constant values of $r_0(t)=r_0$, $\mathrm{CC}_0(t)=\mathrm{CC}_0$, $\Delta\tau_0(t)=\Delta\tau_0$, and $\Delta \ln A_0(t)=\Delta \ln A_0$. We exclude any arrivals before the $P$ wave and after the Rayleigh wave. This is achieved by the box-car function for $w_E(t)$:
%
\begin{align}
w_E(t) & =
@@ -175,7 +175,7 @@
10 w_E & \text{$t > t_{R1}$},
\end{cases}
\end{align}
-%For the \trange{6}{40} data, we exclude any arrivals before the $P$ wave and reduce the number of windows picked beyond R1 by modulating $w_E(t)$.  We use constant values of $r_0(t)=r_0$, $\mathrm{CC}_0(t)=\mathrm{CC}_0$ and $\Delta \ln A_0(t)=\Delta \ln A_0$, but modulate the cross-correlation time lag criterion so that it is less strict at larger epicentral distances and for surface-waves.  We therefore use:
+%For the \trange{6}{30} data, we exclude any arrivals before the $P$ wave and reduce the number of windows picked beyond R1 by modulating $w_E(t)$.  We use constant values of $r_0(t)=r_0$, $\mathrm{CC}_0(t)=\mathrm{CC}_0$ and $\Delta \ln A_0(t)=\Delta \ln A_0$, but modulate the cross-correlation time lag criterion so that it is less strict at larger epicentral distances and for surface-waves.  We therefore use:
%
%\begin{align}
%w_E(t) & =
@@ -192,7 +192,7 @@
%  \end{cases}
%\end{align}

-For the \trange{2}{40} data, we avoid selecting surface-wave arrivals as the 3D model used to calculate the synthetics cannot produce the required complexity. The water-level criteria then becomes:
+For the \trange{2}{30} data, we avoid selecting surface-wave arrivals as the 3D model used to calculate the synthetics cannot produce the required complexity. The water-level criteria then becomes:
%We remove the distance dependence on $\Delta\tau_0(t)$, as higher frequency body-waves are well behaved in this model, and keep all other criteria the same.
%The parameter modulation for these data becomes:
%

===================================================================
(Binary files differ)

===================================================================
--- seismo/3D/ADJOINT_TOMO/flexwin_paper/latex/manual_tuning.tex	2009-03-20 02:15:15 UTC (rev 14400)
+++ seismo/3D/ADJOINT_TOMO/flexwin_paper/latex/manual_tuning.tex	2009-03-20 05:04:47 UTC (rev 14401)
@@ -309,7 +309,7 @@

%CHT modified

-For the \trange{6}{40} and \trange{3}{40} data, we use constant values of $r_0(t)=r_0$, $\mathrm{CC}_0(t)=\mathrm{CC}_0$, $\Delta\tau_0(t)=\Delta\tau_0$, and $\Delta \ln A_0(t)=\Delta \ln A_0$. We exclude any arrivals before the $P$ wave and after the Rayleigh wave. This is achieved by the box-car function for $w_E(t)$:
+For the \trange{6}{30} and \trange{3}{30} data, we use constant values of $r_0(t)=r_0$, $\mathrm{CC}_0(t)=\mathrm{CC}_0$, $\Delta\tau_0(t)=\Delta\tau_0$, and $\Delta \ln A_0(t)=\Delta \ln A_0$. We exclude any arrivals before the $P$ wave and after the Rayleigh wave. This is achieved by the box-car function for $w_E(t)$:
%
\begin{align}
w_E(t) & =
@@ -319,7 +319,7 @@
10 w_E & \text{$t > t_{R1}$},
\end{cases}
\end{align}
-%For the \trange{6}{40} data, we exclude any arrivals before the $P$ wave and reduce the number of windows picked beyond R1 by modulating $w_E(t)$.  We use constant values of $r_0(t)=r_0$, $\mathrm{CC}_0(t)=\mathrm{CC}_0$ and $\Delta \ln A_0(t)=\Delta \ln A_0$, but modulate the cross-correlation time lag criterion so that it is less strict at larger epicentral distances and for surface-waves.  We therefore use:
+%For the \trange{6}{30} data, we exclude any arrivals before the $P$ wave and reduce the number of windows picked beyond R1 by modulating $w_E(t)$.  We use constant values of $r_0(t)=r_0$, $\mathrm{CC}_0(t)=\mathrm{CC}_0$ and $\Delta \ln A_0(t)=\Delta \ln A_0$, but modulate the cross-correlation time lag criterion so that it is less strict at larger epicentral distances and for surface-waves.  We therefore use:
%
%\begin{align}
%w_E(t) & =
@@ -336,7 +336,7 @@
%  \end{cases}
%\end{align}

-For the \trange{2}{40} data, we avoid selecting surface-wave arrivals as the 3D model used to calculate the synthetics cannot produce the required complexity. The water-level criteria then becomes:
+For the \trange{2}{30} data, we avoid selecting surface-wave arrivals as the 3D model used to calculate the synthetics cannot produce the required complexity. The water-level criteria then becomes:

\begin{align}
w_E(t) & =

===================================================================
--- seismo/3D/ADJOINT_TOMO/flexwin_paper/latex/results.tex	2009-03-20 02:15:15 UTC (rev 14400)
+++ seismo/3D/ADJOINT_TOMO/flexwin_paper/latex/results.tex	2009-03-20 05:04:47 UTC (rev 14401)
@@ -6,7 +6,7 @@
tomographic scenarios, with very different geographical extents and distinct period ranges:
long-period global tomography (\trange{50}{150}),
regional tomography of the Japan subduction zone, down to 700~km (\trange{6}{120}), and
-regional tomography of southern California, down to 60~km (\trange{2}{40}).
+regional tomography of southern California, down to 60~km (\trange{2}{30}).
For each of these scenarios, we compare
observed seismograms to spectral-element synthetics, using our
algorithm to select time windows on the pairs of timeseries.