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temperature effect is considered, the tabular expression for GN( φ) should be modified in the following way: ∂GN GN( φ ) = GN( φ ) table + (T0 15°C) ∂T − (8) T 0 is the surface temperature. Fig.2 shows the difference between the atmospheric reduction using 2D data with and without temperature variations. Figure 2 Differences between the attraction effects with and without temperature variation for the reduction using 2D data in Moxa from 2004/01/01 to 2007/12/31 (reduction using (2D with temperature)data – reduction using 2D data) The peak-to-peak amplitude of the difference between both 2D reductions is 0.14 µGal with a dominant seasonal component and it has a RMS value of 0.036 µGal considering a time span of 4 years. 3. Results 3-1 Comparison between the reductions based on 2D and 3D data To develop an optimized barometric pressure reduction suitable for current research related to gravity changes of several days and longer, we investigate how spatially extensive the zone needs to be for which the attraction effect should be computed using 3D data sets. This is done by computing the 3D atmospheric attraction effect around the Moxa station up to 15 ° for 6 zones (Fig.3), respectively the zone from the station to 0.5°, and the ring-shape zone from 0.5° to 1.5°, from 1.5° to 3°, from 3° to 5°, from 5° to 10°, and from 10° to 15°.
a b C d e f Figure 3 Location of Moxa station and considered zones a) up to 0.5° , b) 0.5° - 1.5°, c) 1.5°-3°, d) 3°-5°, e) 5°-10°, f) 10°-15° Fig.4 shows the atmospheric attraction using 3D data for one year from each zone.
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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
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 88 and 89: Figure 4 Attraction effect from the
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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