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1. Introduction The largest uncertainty in predicting the future state of the atmosphere lies in properly estimating the internal changes to the climate system in response to a radiative perturbation ( Cess et al. 1989 ; Cess 2005 ). The impact of these internal changes, commonly called feedbacks on the climate system, can be as large as the primary forcing signal. Perhaps the most important feedback in the earth’s climate system is the climate feedback due to upper-tropospheric water vapor (H
1. Introduction The largest uncertainty in predicting the future state of the atmosphere lies in properly estimating the internal changes to the climate system in response to a radiative perturbation ( Cess et al. 1989 ; Cess 2005 ). The impact of these internal changes, commonly called feedbacks on the climate system, can be as large as the primary forcing signal. Perhaps the most important feedback in the earth’s climate system is the climate feedback due to upper-tropospheric water vapor (H
1. Introduction Water vapor measurements by sun photometry using the 940-nm water vapor absorption band have been compared to in situ and other remote (e.g., microwave) measurements in several previous publications (e.g., Schmid et al. 2000 , 2001 , 2003a , b , 2006 ; Redemann et al. 2003 ; Livingston et al. 2000 , 2003 , 2007 ). Those comparisons were all restricted to sun photometer altitudes <∼6 km, with water vapor columns ∼0.1 to 5 g cm −2 , and water vapor densities ∼0.1 to 17 g
1. Introduction Water vapor measurements by sun photometry using the 940-nm water vapor absorption band have been compared to in situ and other remote (e.g., microwave) measurements in several previous publications (e.g., Schmid et al. 2000 , 2001 , 2003a , b , 2006 ; Redemann et al. 2003 ; Livingston et al. 2000 , 2003 , 2007 ). Those comparisons were all restricted to sun photometer altitudes <∼6 km, with water vapor columns ∼0.1 to 5 g cm −2 , and water vapor densities ∼0.1 to 17 g
1. Introduction Below the melting point, the equilibrium vapor pressure (hereafter referred to simply as vapor pressure) of liquid water exceeds that of ice at the same temperature. Because of that difference in vapor pressure, in clouds, once any droplet freezes, it grows by condensation at the expense of surrounding droplets that have not frozen. To calculate the rate at which the mass transfer proceeds, both vapor pressures must be known as it is the difference (i.e., gradient) that drives
1. Introduction Below the melting point, the equilibrium vapor pressure (hereafter referred to simply as vapor pressure) of liquid water exceeds that of ice at the same temperature. Because of that difference in vapor pressure, in clouds, once any droplet freezes, it grows by condensation at the expense of surrounding droplets that have not frozen. To calculate the rate at which the mass transfer proceeds, both vapor pressures must be known as it is the difference (i.e., gradient) that drives
1. Introduction Water vapor is the most important natural greenhouse gas of the atmosphere and has a large impact on its radiative properties and hence on its thermodynamic balance. Despite the importance of water vapor in the climate system and weather forecasting, there is no technique available, neither ground-based nor spaceborne, that can provide continuous measurements of the humidity profile under all weather conditions. Ground-based microwave radiometers measuring the pressure
1. Introduction Water vapor is the most important natural greenhouse gas of the atmosphere and has a large impact on its radiative properties and hence on its thermodynamic balance. Despite the importance of water vapor in the climate system and weather forecasting, there is no technique available, neither ground-based nor spaceborne, that can provide continuous measurements of the humidity profile under all weather conditions. Ground-based microwave radiometers measuring the pressure
1. Introduction A number of studies indicate that moist convection is sensitive to free-tropospheric water vapor, including observational analyses ( Austin 1948 ; Malkus 1954 ; Brown and Zhang 1997 ; Sherwood 1999 ; Parsons et al. 2000 ; Bretherton et al. 2004 ; Sherwood et al. 2004 ) and studies using cloud-system-resolving models (CSRMs; Tompkins 2001b ; Grabowski 2003 ; Derbyshire et al. 2004 ). This dependence is apparently not well represented in global climate models ( Derbyshire
1. Introduction A number of studies indicate that moist convection is sensitive to free-tropospheric water vapor, including observational analyses ( Austin 1948 ; Malkus 1954 ; Brown and Zhang 1997 ; Sherwood 1999 ; Parsons et al. 2000 ; Bretherton et al. 2004 ; Sherwood et al. 2004 ) and studies using cloud-system-resolving models (CSRMs; Tompkins 2001b ; Grabowski 2003 ; Derbyshire et al. 2004 ). This dependence is apparently not well represented in global climate models ( Derbyshire
earth. The range is relatively narrow and oriented perpendicular to the flow. The zone would undoubtedly make an excellent ‘laboratory’ for the verification of theoretical models of airflow over mountain and the resulting precipitation and cloudiness patterns.” The goal of this study is to determine the isotope fractionation of water vapor crossing the southern Andes and to use this information to estimate the drying ratio and test and calibrate a physical model of orographic precipitation. Because
earth. The range is relatively narrow and oriented perpendicular to the flow. The zone would undoubtedly make an excellent ‘laboratory’ for the verification of theoretical models of airflow over mountain and the resulting precipitation and cloudiness patterns.” The goal of this study is to determine the isotope fractionation of water vapor crossing the southern Andes and to use this information to estimate the drying ratio and test and calibrate a physical model of orographic precipitation. Because
been proposed to play a role in Arctic amplification include the water vapor feedback, since a warmer atmosphere can hold more water vapor (which is a greenhouse gas), as well as cloud feedbacks and poleward heat transport in both the atmosphere and ocean (e.g., Holland and Bitz 2003 ; Alexeev et al. 2005 ; Francis and Hunter 2006 ; Kay and Gettelman 2009 ; Hwang et al. 2011 ; Mahlstein and Knutti 2011 ; Alexeev and Jackson 2013 ; Goosse et al. 2018 ; Beer et al. 2020 ). Studies of
been proposed to play a role in Arctic amplification include the water vapor feedback, since a warmer atmosphere can hold more water vapor (which is a greenhouse gas), as well as cloud feedbacks and poleward heat transport in both the atmosphere and ocean (e.g., Holland and Bitz 2003 ; Alexeev et al. 2005 ; Francis and Hunter 2006 ; Kay and Gettelman 2009 ; Hwang et al. 2011 ; Mahlstein and Knutti 2011 ; Alexeev and Jackson 2013 ; Goosse et al. 2018 ; Beer et al. 2020 ). Studies of
1. Introduction Raman lidar is now regarded as one of the leading technologies for atmospheric profiling of water vapor ( Melfi et al. 1989 ; Whiteman et al. 1992 ; Goldsmith et al. 1998 ; Turner et al. 2000 ), cirrus clouds ( Ansmann et al. 1992a ; Reichardt et al. 2002 ; Whiteman et al. 2004 ), aerosols ( Ansmann et al. 1990 ; Ferrare et al. 2006 ), temperature ( Arshinov et al. 2005 ; Behrendt et al. 2002 ; Di Girolamo et al. 2004 ), and other atmospheric constituents or properties
1. Introduction Raman lidar is now regarded as one of the leading technologies for atmospheric profiling of water vapor ( Melfi et al. 1989 ; Whiteman et al. 1992 ; Goldsmith et al. 1998 ; Turner et al. 2000 ), cirrus clouds ( Ansmann et al. 1992a ; Reichardt et al. 2002 ; Whiteman et al. 2004 ), aerosols ( Ansmann et al. 1990 ; Ferrare et al. 2006 ), temperature ( Arshinov et al. 2005 ; Behrendt et al. 2002 ; Di Girolamo et al. 2004 ), and other atmospheric constituents or properties
1. Introduction A gain of water in the soil surface layer, not caused by rainfall or irrigation, can be caused by dew deposition or vapor adsorption. Dew deposition is a phenomenon recorded for most soil and climate types ( Jacobs et al. 1994 , 1999 ). It occurs during the night when dewpoint is reached, and it results in a discernable wetting of the surface ( Monteith 1957 ). Vapor adsorption is an important phenomenon in arid and semiarid regions ( Kosmas et al. 1998 , 2001 ; Agam and
1. Introduction A gain of water in the soil surface layer, not caused by rainfall or irrigation, can be caused by dew deposition or vapor adsorption. Dew deposition is a phenomenon recorded for most soil and climate types ( Jacobs et al. 1994 , 1999 ). It occurs during the night when dewpoint is reached, and it results in a discernable wetting of the surface ( Monteith 1957 ). Vapor adsorption is an important phenomenon in arid and semiarid regions ( Kosmas et al. 1998 , 2001 ; Agam and
Variability of Water Vapor in Central Mexico from Two Remote Sensing Techniques: FTIR Spectroscopy and GPSvapour profiles in the framework of the Total Carbon Column Observing Network (TCCON) . Atmos. Meas. Tech. , 3 , 1785 – 1795 , https://doi.org/10.5194/amt-3-1785-2010 . 10.5194/amt-3-1785-2010 Semenov , A. O. , Y. A. Virolainen , Y. M. Timofeyev , and A. V. Poberovskii , 2015 : Comparison of ground-based FTIR and radio sounding measurements of water vapor total content . Atmos. Oceanic Opt. , 28 , 121 – 125 , https://doi.org/10.1134/S1024856015020116 . 10.1134/S1024856015020116
vapour profiles in the framework of the Total Carbon Column Observing Network (TCCON) . Atmos. Meas. Tech. , 3 , 1785 – 1795 , https://doi.org/10.5194/amt-3-1785-2010 . 10.5194/amt-3-1785-2010 Semenov , A. O. , Y. A. Virolainen , Y. M. Timofeyev , and A. V. Poberovskii , 2015 : Comparison of ground-based FTIR and radio sounding measurements of water vapor total content . Atmos. Oceanic Opt. , 28 , 121 – 125 , https://doi.org/10.1134/S1024856015020116 . 10.1134/S1024856015020116
