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, concluding that the “most scientifically sound projection is that PMP values will increase in the future.” Regional climate model simulations in the Kansas–Oklahoma area of Zhao et al. (1997) , which were designed to examine the “moisture maximization” assumptions linking precipitable water to PMP, point to pronounced changes in storm structure with increasing humidity and nonlinear relationships between precipitable water and maximum rainfall. The Great Plains low-level jet has been identified as a key
, concluding that the “most scientifically sound projection is that PMP values will increase in the future.” Regional climate model simulations in the Kansas–Oklahoma area of Zhao et al. (1997) , which were designed to examine the “moisture maximization” assumptions linking precipitable water to PMP, point to pronounced changes in storm structure with increasing humidity and nonlinear relationships between precipitable water and maximum rainfall. The Great Plains low-level jet has been identified as a key
; Hou et al. 2014 ) core satellite. Our study focuses on atmospheric rivers (ARs) and rainfall during the IFloodS period. ARs are narrow (less than 400 km in width) and long (1000+ km in length) regions in the lower levels of the troposphere that transport large amounts of water vapor from the tropics and extratropics ( Newell et al. 1992 ; Newell and Zhu 1994 ). In extratropical cyclones, ARs generally form in the warm sector in the presence of low-level jets (LLJs) ahead of cold fronts. Because
; Hou et al. 2014 ) core satellite. Our study focuses on atmospheric rivers (ARs) and rainfall during the IFloodS period. ARs are narrow (less than 400 km in width) and long (1000+ km in length) regions in the lower levels of the troposphere that transport large amounts of water vapor from the tropics and extratropics ( Newell et al. 1992 ; Newell and Zhu 1994 ). In extratropical cyclones, ARs generally form in the warm sector in the presence of low-level jets (LLJs) ahead of cold fronts. Because
case when the data from all the instruments were available. This event was a mixture of stratiform and convective echoes associated with a mesoscale convective system (MCS). The convection began to build in the early morning (0700 UTC) on 26 May along the low-level jet to the south and west of XPOL-5. The XPOL-5 region witnessed the mixture of stratiform and convective systems until 1900 UTC, with the most intense echoes covering most of XPOL-5 region between 1100 and 1300 UTC and 1500 and 1800 UTC
case when the data from all the instruments were available. This event was a mixture of stratiform and convective echoes associated with a mesoscale convective system (MCS). The convection began to build in the early morning (0700 UTC) on 26 May along the low-level jet to the south and west of XPOL-5. The XPOL-5 region witnessed the mixture of stratiform and convective systems until 1900 UTC, with the most intense echoes covering most of XPOL-5 region between 1100 and 1300 UTC and 1500 and 1800 UTC
