Aftershock Blue Cool Citrus Liqueur, 70 cl

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In August 2008, it was announced that the Alcohol Content (abv) would be lowered to 30%, from 40%. It was also announced that the Green variant (Thermal Bite) would be discontinued. Li, S. & Freymueller, J. T. Spatial variation of slip behavior beneath the Alaska Peninsula along Alaska-Aleutian subduction zone. Geophys. Res. Lett. 45, 3453–3460 (2018). Bai, Y., Ye, L., Yamazaki, Y., Lay, T. & Cheung, K. F. The 4 May 2018 M W 6.9 Hawaii Island earthquake and implications for tsunami hazards. Geophys. Res. Lett. 45, 11,040–11,049 (2018).

An upper plate splay-fault model for the additional source of tsunami waves involves a compact 20 km × 30 km slip patch with an upper edge 3 km deep, and strike 250°, dip 35°, and rake 90°, with 12 m of pure thrust slip. The slow-fault ruptures at the same time as the initiation of the earthquake and lasts for 5 min. Assuming a rigidity of 30 GPa, appropriate for the shallow megathrust environment, the seismic moment is 2.16 × 10 20 Nm ( M W 7.49). The computed seafloor deformations for the two-fault coseismic rupture and the slow thrust slip on the splay patch are shown in Supplementary Fig. 10, separately and combined. The thrust splay patch is located near the shelf break and similar to the dipole fitting has about 20 km absolute uncertainty, but cannot locate significantly out onto the continental slope, as the tsunami excitation changes rapidly along the slope and incompatible waveforms are produced at the DART stations. The resulting seafloor deformation again resembles a scaled-up version of the 2-fault model with uplift and subsidence straddled across the shelf break. Comparisons of the observed and computed tsunami signals for the three-fault model are shown in Supplementary Fig. 11, with clear uniform improvement relative to the two-fault solution in Fig. 4. The fits are slightly improved in comparison to those for the optimal megathrust slow-slip model in Supplementary Fig. 9. The large second arrival and the following trough in the DART waveforms are matched well by the slow-slip event. The computed tsunami waves from the two sources are out-of-phase in Hawaii waters and the matching with the tide gauge records through destructive interference is remarkable (Supplementary Fig. 11). Again, we reject this specific model despite its ability to match the tsunami data because it predicts larger dynamic displacements at GNSS stations AC12 and AC28 (Supplementary Fig. 10), which are not observed after the motions from the fast rupture. Coulomb failure stress Herman, M. W. & Furlong, K. P. Triggering an unexpected earthquake in an uncoupled subduction zone. Sci. Adv. 7, eabf7590 (2021).Ye, L., Lay, T. & Kanamori, H. The 25 March 2020 M W 7.5 Paramushir, northern Kuril Islands earthquake and major ( M W ≥7.0) near-trench intraplate compressional faulting. Earth Planet. Sci. Lett. 556, 116728 (2021). Shillington, D. J., Bécel, A. & Nedimovíc, M. R. Upper plate structure and megathrust properties in the Shumagin Gap near the July 2020 M7.8 Simeonof event. Geophys. Res. Lett. 49, e2021GL096974 (2022). We select 62 P and 50 SH broadband recordings from the Incorporated Research Institutions for Seismology (IRIS) data management center with well-distributed azimuthal coverage at teleseismic epicentral distances between 30° and 90° (station distributions and data are shown in Supplementary Fig. 3). Instrument responses are removed to obtain ground velocities in the passband 1–300 s with waveform durations of 100 s. We precisely aligned P and SH wave initial motions manually.

Ye, L. et al. Rupture model for the 29 July 2021 M W 8.2 Chignik, Alaska earthquake constrained by seismic, geodetic, and tsunami observations. J. Geophys. Res.: Solid Earth 127, e2021JB023676 (2022). Ji, C., Helmberger, D. V., Wald, D. J. & Ma, K. F. Slip history and dynamic implications of the 1999 Chi‐Chi, Taiwan, earthquake. J. Geophys. Res.: Solid Earth 108, 2412 (2003).

Given the guidance provided by the simple dipole modeling, we considered physical fault dislocation models for plausible geometries that can match the salient features of seafloor deformation from the dipole model that leads to successful match of the tsunami waveforms. This includes simultaneous assessment of the seismic and geodetic motions produced by such models for the sensitive high-rate GNSS recordings at nearby stations AC12 and AC28. The latter constraint is very important; there is essentially no geodetic or seismic signature of the second (dominant) tsunami source, and models that violate this can be rejected with confidence. We considered appropriately placed models with delayed slow thrust slip on the shallow megathrust (Methods, Supplementary Figs. 8, 9) or slow thrust slip on an upper plate splay fault with a strike parallel to the trench (Methods, Supplementary Figs. 10, 11) and allowed sufficiently long source process times to obscure the seismic and geodetic expressions while giving strong tsunami excitation, finding models that match the tsunami signals by extensive searches over model parameters (fault dimensions, slip, absolute location, etc.). However, those models that do match the tsunami observations acceptably all badly violate the geodetic observations at AC12 and AC28 (Supplementary Figs. 8, 10). This eliminates the more obvious candidate model geometries. Successful slow-slip faulting geometry The table below contains all postcodes on a two day service. Please note all deliveries to Northern Ireland are also on a 3-5 days service.