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Figure 7 Atmospheric reductions for Moxa observatory from 2004/01/01 to 2007/12/31 (3D+2D) data = attraction effect : based on 3D data up to 5 degree around station + 2D data are used for the calculation of the rest of the Earth deformation effect : based on 2D data 2D data = attraction and deformation effect : based on 2D data Admittance = the reduction based on admittance factor The reduction using an admittance factor is larger than the others. The difference between the reductions is given in Fig.8 for the same 4 year-long data set.
Figure 8 Differences between atmospheric reductions from 2004/01/01 to 2007/12/31 a) based on 3D+2D data - 2D data b) based on 3D+2D - admittance factor c) based on 2D data - admittance factor The difference between the two reductions based on a physical approach (Fig.8a) has a peak-to-peak amplitude of 0.5 µGal including seasonal variations with an amplitude of 0.15 µGal as mentioned previously with a maximum in summer. The RMS value amounts to 0.1 µGal. Fig.8b, c show respectively the differences between the reductions derived from the two physical approaches and an admittance factor. They have similar variations and a peak-to-peak amplitude of 3 µGal with a RMS value of 0.4 µGal. In order to determine, in which spectral ranges the differences occur, spectral analyses are computed (Fig.9).
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MAREES TERRESTRES BULLETIN D'INFORM
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BIM 146 December 15, 2010 New Chall
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1994), and TPXO.6 (Egbert et al., 1
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4. An attempt to improve the region
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From Fig. 2, we also see that, the
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GPS network called GEONET (GPS Eart
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References Bos, M. S., Baker, T. F.
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Planets Space, 59, 307-311. Sato, T
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Fig. 1. Locations of the observatio
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the dense seismic observation netwo
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difference of loading effects of oc
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is done with an optical lever using
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6. Application of laser interferome
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Figure 11. Strain seismograms of th
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Higashi, T., 1996, A study on chara
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2. Fundamentals and techniques At t
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100 low frequencies earth tide freq
Page 42 and 43: Tab. 4: Averages of noise levels at
Page 44 and 45: References Asch, G., Elstner, C., J
Page 46 and 47: The 1 / s part is also worth mentio
Page 48 and 49: As it was mentioned before the resu
Page 50 and 51: Fig. 9. Morlet Wavelet Spectrum, su
Page 52 and 53: 9. CONCLUSIONS This investigation w
Page 54 and 55: 2. Objectives of Aswan Tidal Gravit
Page 56 and 57: 5. Recording of Data The data logge
Page 58 and 59: Figure 5: Pre-processed hourly data
Page 60 and 61: Figure 6: Residuals of gravity tide
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Page 64 and 65: time. In addition, models for gravi
Page 66 and 67: Fig. 3 (Zahran, 2005) shows gravity
Page 68 and 69: during the years 2003 and 2004. It
Page 70 and 71: Figure 7: Variation of phase shift,
Page 72 and 73: Figure 8: Induced gravity load and
Page 76 and 77: The instrumentation of the tidal st
Page 78 and 79: 4. Tidal analysis The tidal analysi
Page 80 and 81: References Banka, D., Crossley, D.
Page 82 and 83: 1. Introduction The estimation of a
Page 84 and 85: Figure 1 Air density distributions
Page 86 and 87: temperature effect is considered, t
Page 88 and 89: Figure 4 Attraction effect from the
Page 90 and 91: a ) up to 0.5° , b) 0.5°- 1.5° ,
Page 94 and 95: Figure 9 Amplitude spectra of diffe
Page 96 and 97: Figure 10 SG observation and gravit
Page 98 and 99: eduction in the long-period tides r
Page 100 and 101: oceans. The effect has a peak-to-pe
Page 104 and 105: Figure 1. Local earthquakes recorde
Page 106 and 107: 4. Recording of Data The recorded d
Page 108 and 109: Table 1: Adjusted tidal parameters
Page 110 and 111: Acknowledgements: The authors are i
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