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Figure 4 Attraction effect from the zones indicated in Fig.2 computed with 3D data from 2007/01/01 to 2007/12/31 (different scaling) a ) up to 0.5° , b) 0.5°- 1.5° , c) 1.5°- 3.0° , d) 3.0°- 5.0° , e) 5.0° - 10.0° , e) 10.0°- 15.0° For the innermost zone the maximal amplitude of attraction effect is around 20 µGal and the Root Mean Square (RMS) value is 3.19 µGal. The peak-to-peak effect from the zone of 0.5° - 1.5° is roughly 1/7 of the innermost zone and the contribution from the zone of 1.5° - 3° reaches 1/30 of the innermost zone. The amplitude of the attraction effect from the zone of 3° - 5° has a peak-to-peak amplitude of 0.3 µGal (Fig.6d), a RMS value of 0.06 µGal and the effect from this zone is the smallest one. The variations from the zone of 5° - 10° and 10° - 15°
evert in sign. The reason for this is that due to the Earth’s curvature, the attraction effect around the zone of 3° - 5° is nearly at the same height level as the gravity meter. The attraction from the zone which is more than 5° from the gravity station is already below the height level of the gravity meter. Thus, the direction of the attraction effect changes in sign. These characteristics are also visible in the tabulated Green’s functions in Merriam (1992). In order to estimate for which area the attraction effect using 3D data should be computed, a reduction based on 2D surface data (pressure and temperature) from ECMWF and a standard atmosphere is calculated for comparison (Fig.5). Figure 5 Attraction effect from the zones indicated in Fig.2 computed with 2D with temperature data from 2007/01/01 to 2007/12/31 (different scaling)
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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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Page 38 and 39: 2. Fundamentals and techniques At t
Page 40 and 41: 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 90 and 91: a ) up to 0.5° , b) 0.5°- 1.5° ,
Page 92 and 93: Figure 7 Atmospheric reductions for
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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