Responses and impacts of atmospheric rivers to climate change


Atmospheric rivers (ARs) are characterized by intense moisture transport, which, on landfall, produce precipitation which can be both beneficial and destructive. ARs in California, for example, are known to have ended drought conditions but also to have caused substantial socio-economic damage from landslides and flooding linked to extreme precipitation. Understanding how AR characteristics will respond to a warming climate is, therefore, vital to the resilience of communities affected by them, such as the western USA, Europe, East Asia and South Africa. In this Review, we use a theoretical framework to synthesize understanding of the dynamic and thermodynamic responses of ARs to anthropogenic warming and connect them to observed and projected changes and impacts revealed by observations and complex models. Evidence suggests that increased atmospheric moisture (governed by Clausius–Clapeyron scaling) will enhance the intensity of AR-related precipitation — and related hydrological extremes — but with changes that are ultimately linked to topographic barriers. However, due to their dependency on both weather and climate-scale processes, which themselves are often poorly constrained, projections are uncertain. To build confidence and improve resilience, future work must focus efforts on characterizing the multiscale development of ARs and in obtaining observations from understudied regions, including the West Pacific, South Pacific and South Atlantic.

Key points

  • Atmospheric rivers are important components of the meridional transport of atmospheric moisture. They influence the hydroclimate of a number of regions in the mid-latitudes.

  • On land, atmospheric rivers are the source of both beneficial water resources and deleterious hazards (mudslides, floods and, in their absence on longer timescales, droughts).

  • The robust thermodynamic response of atmospheric moisture to climate change means that future atmospheric rivers will contain more moisture, but circulation changes and potential decreases in their precipitation efficiency must be considered in future impact studies.

  • At the global scale, much is still unknown about atmospheric rivers, including basic observations of their development, their interaction with large-scale dynamics and their role in short-duration, high-volume melt events over the Arctic and Antarctic.

  • Future research on the mechanisms driving atmospheric rivers and their life cycles will be a critical advancement for further quantifying their response to climate change.


Atmospheric rivers (ARs) are synoptic-scale features characterized by their striking geometry — extending thousands of kilometres in length and an order of magnitude less in width1 — and vertically coherent low-level moisture transport concentrated in the bottom 3 km of the atmosphere2 (Fig. 1). In total, ARs are estimated to accomplish as much as 90% of poleward moisture transport3,4, which, in the North Pacific, averages 700 kg m−1 s−1 (Fig. 1b), more than twice the mean annual discharge found at the mouth of the Amazon River5. ARs do not describe continuous moisture transport. Rather, they are continually evolving pathways that incorporate moisture from local convergence and evaporation along their track6,7 or, in select cases, from distant source regions in the tropics or subtropics8,9,10,11,12. Owing to the complexity of their evolution, our baseline knowledge of AR characteristics at the global scale is uncertain due to the dependency on identification algorithms (Box 1), with factors such as genesis, development and termination only recently being explored13,14.

Fig. 1: Characteristics of a typical atmospheric river.

a | A plan view of the typical structure and orientation of an atmospheric river (AR). b | Vertical cross section through the core of the AR (A–A′). Green contours show the water vapour mixing ratio, red contours show water vapour transport and blue contours show the wind speed. c | An example of a strong landfalling AR from the Pacific Northwest on 06 November 2006 in ERA5 reanalysis data. Black contours show the magnitude of vertically integrated heat flux in units of W m−1 co-located with the AR, drawn at intervals of 0.05 × 1011 W m−1. Coloured contours depict 2-m surface temperature, drawn at intervals of 2 K. IVT, integrated vapour transport. Adapted with permission from ref.5, American Meteorological Society.

However, ARs are known to operate as one part of a larger, synoptic-scale dynamical system driving the poleward transport of sensible and latent heat4,15. They are generally found in the vicinity of extratropical cyclones. Over the North Pacific, for example, 85% of ARs are paired with extratropical cyclones16, consistent with their observed relationship with baroclinic instabilities and the mid-latitude storm track3,6. However, this relationship is nuanced; only 45% of extratropical cyclones over the same region are associated with an AR16. Similar non-linear relationships are observed in the North Atlantic, where the evolution and life cycle of a single AR can span that of several cyclones9. While the phenomena are clearly related, their relationship is interactive, with potential implications on the intensification of storms and the severity of precipitation impacts on land17,18.

Indeed, given their intense moisture transport and moist-neutrality, ARs exhibit conditions that are ideal for forced precipitation, either through interaction with topography or ascent along a warm conveyor belt or frontal boundary19. Thus, when ARs make landfall, they can have a range of hydrological impacts, including precipitation extremes and related hazards, as well as contributions to water supplies20,21,22,23,24. For example, ARs provide 20–30% of annual precipitation in western Europe and the western USA22, and 14–44% of warm-season total precipitation in East Asia25.

With 4–5 ARs present in each hemisphere at any point in time3, their influence is felt globally. Nevertheless, AR-related impacts are largely constrained to the western coastlines of South America26,27,28, South Africa29, North America30 and Europe31,32,33,34,35,36, the eastern coastlines of Japan25,37 and New Zealand38,39, and over continental regions, such as the Central and Eastern United States40,41,42. Emerging research has also found AR-like structures over the western Mediterranean that share some characteristics with ARs in the mid-latitudes and contribute to precipitation extremes43. Moreover, ARs extend into the polar regions44,45,46,47, where the increased temperatures and moisture that accompany these events further modify an environment already sensitive to feedback processes48. ARs, for example, have been observed to amplify summertime warming in the Arctic troposphere49, influence the decline of Arctic sea ice by affecting the surface radiative balance50 and bring about mass surface-melt events in West Antarctica, with the circulation patterns that accompany them51.

Multiple factors contribute to the scale of the impacts ARs have at landfall, including duration over space and time, the temperature and intensity of moisture transport and antecedent soil moisture and snowpack conditions52,53,54. The rapid succession of individual landfalling ARs over a short period (less than a week) can supplant the initially beneficial supply of water resources. These AR ‘families’ are modulated by large-scale dynamics55,56 and are most notably linked to the events leading to damage of the Oroville Dam in February 2017 (ref.57). Evidence of megaflood events in the palaeoclimate record in the West Coast of the United States, likely linked to landfalling AR events, suggests that the full range of their variability is still unknown58,59.

Communities experience detrimental effects related to ARs through impacts on water resources and hazards, either primary or secondary, to extreme precipitation. The robust increase of atmospheric moisture and potential for changes in large-scale circulation with climate change have implications on the intensity, moisture sources and preferred tracks of future ARs. However, it is not enough to connect increases in the intensity of moisture transport to changes in hydrological hazards when they make landfall. The precipitation associated with ARs can respond quite differently from changes seen in moisture transport and are reliant on not only surface processes such as orographic forcing but also the location, duration and intensity of moisture transport within ARs. These changes may manifest in even more extreme AR events and exacerbate current difficulties in water management. Vital to the resilience of communities affected by ARs is knowing how their characteristics will respond to a warming climate.

In this Review, we present a comprehensive synthesis of AR responses to warming, connecting the theoretical basis for changes in ARs to results from complex models and observations. Building on theory, we first explore how thermodynamic and dynamic responses to warming affect the scale of AR impacts on land. We subsequently provide an overview of the observed and projected changes to AR characteristics, including their impacts, followed by an assessment of future research priorities. The multiple roles ARs play in the climate system and the complexity of their impacts at landfall motivate the importance of a holistic approach.

Theory-based changes to atmospheric rivers

The unique characteristics that comprise ARs provide opportunities to examine a subset of precipitation producers in a future climate from a conceptual perspective. We begin by discussing the physical theory associated with AR responses to idealized warming, focusing on their most defining feature, intense moisture transport. AR intensity is captured by the column-integrated water-vapour transport (IVT),

$$IVT={g}^{-1}\sqrt{{\left({\int }_{{p}_{{\rm{s}}}}^{{p}_{{\rm{t}}}}qu{\rm{d}}p\right)}^{2}+{\left({\int }_{{p}_{{\rm{s}}}}^{{p}_{{\rm{t}}}}qv{\rm{d}}p\right)}^{2}}$$

where g is standard gravity, u and v the zonal and meridional winds, respectively, q specific humidity, ps surface pressure and pt an upper-atmospheric reference pressure (typically set between 500 and 200 hPa). For simplicity, we define IVT as the magnitude of water-vapour transport, but vector definitions also appear in the literature5. As specific humidity changes as a function of temperature and pressure alone under saturated conditions typical of ARs, IVT offers a valuable investigative framework for understanding ARs. Indeed, changes in IVT can be decomposed into distinct contributions from thermodynamics (the change in atmospheric moisture content, q) and dynamics (the change in atmospheric motion, u and v), each of which is now discussed.

Thermodynamic responses

A natural starting point for understanding the change in the thermodynamic component of IVT is the Clausius–Clapeyron equation, which states that the water-vapour content of saturated air, q, increases nearly exponentially with temperature T according to

$$\frac{{\rm{d}}{q}^{\ast }}{{\rm{d}}T}=\alpha (T){q}^{\ast }.$$

α(T) is the Clausius–Clapeyron scaling factor, defined as

$$\alpha (T)=\frac{L}{{R}_{v}{T}^{2}},$$

where L is the latent heat of vaporization and Rv is the gas constant of water vapour. Within the saturated environment at the core of an AR (where q ≈ q), Eq. (2) implies that the fractional change in humidity per degree of surface warming ΔTs is approximately given by

$$\frac{1}{\Delta {T}_{{\rm{s}}}}\frac{\Delta q}{q}=\alpha (T)\frac{\Delta T}{\Delta {T}_{{\rm{s}}}},$$

where ΔTTs represents the magnitude of warming at a particular height relative to the surface. At the surface, where ΔT = ΔTs, specific humidity scales with temperature at the rate of the Clausius–Clapeyron scaling factor, α(Ts). This scaling is approximately 6.6% K−1 for surface temperatures characteristic of ARs making landfall in California in the present climate (Ts = 13 °C (refs52,60)).

Above the surface, however, the IVT response to warming is complicated by two factors. First, α is not constant but varies with temperature from ~6% K−1 in the tropical boundary layer to >7% K−1 at temperatures below freezing61. Given that temperature decreases with height, α is, therefore, larger in the upper troposphere than at the surface, amplifying the change in specific humidity (q) aloft61. Second, an increase in q results in more latent heat being released as saturated air ascends, in turn decreasing the lapse rate with warming and, thus, increasing ΔT with height61,62,63. Under the saturated, moist-neutral conditions of an AR, the combination of these factors implies a rate increase in column-integrated water vapour that is substantially larger than that of near-surface water vapour: 9.5% K−1 compared with 6.6% K−1 when Ts = 13 °C (ref.52)). While the larger increase in IVT relative to surface water vapour has been described as super-Clausius–Clapeyron scaling64, it is, in fact, a straightforward consequence of Clausius–Clapeyron scaling applied to a saturated, moist-neutral environment. Therefore, the fractional change in integrated water vapour is a reasonable approximation to the thermodynamic contribution to IVT change64,65,66.

The vertical distribution of water vapour, wind speed and, consequently, water-vapour transport within ARs is another factor subject to change in future climate scenarios. Mid-level water-vapour transport, for example, is an important process producing heavy precipitation on the lee side of the northern Sierra Nevada67,68. These studies have a specific regional focus; however, the importance of mid-level transport in extending AR conditions inland of major topographic barriers can be generalized to many regions. Water vapour transported above the crest level is less likely to be lost due to forced ascent and rainout on the windward side of such barriers. Accurately modelling changes in the vertical distribution of water-vapour transport is critical to predicting future hydroclimate, particularly over interior continental regions positioned downstream of topography.

Dynamical responses

In contrast to expected thermodynamic responses, the response of atmospheric circulation to warming is much less certain69,70. As a consequence, our discussion of dynamical responses of IVT is broader and focused on two aspects that are vitally important to the impact of ARs on land: their location of landfall and intensity. These aspects are modified by changes in the large-scale circulation patterns and by the energetics of the atmosphere.

Uncertainty in the mid-latitude-circulation response originates from the many competing influences on the location of the eddy-driven jet in a warming climate system71. The jet stream is the guide against which cyclones propagate and, consequently, is closely related to the location of ARs and the high IVT that characterizes them. In the upper atmosphere, moistening of the tropical troposphere leads to increased latent-heat release and amplified warming relative to the lower troposphere. In the lower atmosphere, declining sea ice and other feedback processes act to amplify surface-temperature increase in the polar region72,73. These changes have opposing effects on the meridional temperature gradient, so that the temperature gradient increases in the upper troposphere and decreases in the lower troposphere. Shifts in the eddy-driven jet with climate change depend on this ‘tug-of-war’ between the two responses74 and, thereby, remains a significant source of uncertainty for diagnosing changes in precipitation patterns75,76.

The preceding description is a much-simplified picture of the complex and interwoven mechanisms that influence the response of large-scale dynamics to warming77. Regional differences in the responses of the jet are certain78; however, generally, models show a poleward shift in the eddy-driven jet, which leads to increased static stability in the subtropics79,80 and upward expansion of the storm track, all consistent with an increase in the upper-level meridional temperature gradient71,81,82. The response of the eddy-driven jet will shift future ARs poleward66. Those events occurring at lower latitudes may also be shifted equatorward, depending on the location and strength of the subtropical jet shift, which shows a similar poleward shift and strengthening with warming79.

Against this simplified framework, several competing effects may influence the intensity of IVT. Increased atmospheric moisture with warming drives the increase of latent-heat release and, consequently, the intensification of IVT and associated extratropical cyclones83. At the same time, a reduction in the baroclinic instability due to a decrease in the meridional temperature gradient and increased efficiency of poleward moisture transport in a moister atmosphere may reduce the moisture transport84.

The separation between potential moisture sources may influence the sources of moisture contained within ARs. Over the eastern North Pacific, while over 70% of moisture within ARs was found to be locally sourced, at least 15% was found to be subtropical or tropical in origin85.

Precipitation responses

In climate models, there is a robust increase in global mean precipitation; however, how the response of ARs contributes towards this change is still uncertain and depends on many more factors than increased moisture alone86. In this section, we examine how the previously discussed thermodynamic and dynamic responses of IVT contribute to changes in AR-related precipitation patterns.

In regions with little topographic relief, the local precipitation rate, P, is approximately equal to the column-integrated condensation rate during a strong landfalling AR event with large IVT,

$$P\approx {\int }_{0}^{{p}_{{\rm{s}}}}\omega \frac{{\rm{d}}q}{{\rm{d}}p}{\left | \right. }_{{\theta }_{{\rm{e}}}}{\rm{d}}p,$$

where ω is the vertical velocity in pressure coordinates, dq/dp the vertical gradient in specific humidity following a moist adiabat and θe the equivalent potential temperature. Given that moist-neutral stratification is a general characteristic of strong ARs, ω is not expected to change much under warming87. For a generally strong AR event in which ascent extends through the full depth of the troposphere, constant ω therefore implies that P will scale with warming at roughly the same rate as near-surface q (that is, ΔP/(PΔTs) ≈ α(Ts)). Consequently, precipitation from ARs will increase at a lower rate than IVT under warming. For example, in a comparison of the historical period to end-of-the-century Representative Concentration Pathway 8.5 (RCP 8.5) in a large ensemble of model simulations, the number of extreme-precipitation AR days increased by 28%, compared with 35% for the total number of AR days88.

In many regions, however, orographic processes will act to enhance AR-related precipitation through interactions between the large-scale flow and local topography. In the Sierra Nevada mountain range of California, for example, windward slopes receive around four times more precipitation during ARs compared with lower elevations upstream. Similar examples of orographic-precipitation enhancement are also observed in Norway31,89, New Zealand39, Japan25 and much of the western coastlines of North90,91,92 and South America27,28,93. In these and other mountainous regions, orographic processes could strongly influence the response of AR precipitation to warming.

Recent studies have identified several mechanisms that could affect the amount and distribution of AR precipitation in mountainous regions under warming. For example, due to basic thermodynamics, the vertical structure of condensation over a mountain’s windward slope will shift upward with warming, essentially requiring air to be lifted higher to reach condensation61. This process shifts the spatial pattern of precipitation downwind and drives a sub-Clausius–Clapeyron increase (an increase of 9.3% compared with non-orographic precipitation at 13.1%) in the total precipitation across the mountain. While regional-climate-model simulations provide some evidence of these thermodynamic effects94,95, other changes, such as mountain-wave dynamics96 and hydrometeor growth and fallout63,97,98, are also thought to influence AR-precipitation responses. This complexity points to the need for further analysis of the mechanisms governing orographic precipitation and its response to climate change — an effort that will be substantially aided by greater availability of high-resolution simulations99 (Box 2).

Theory further suggests that an increase in water-vapour transport above crest level, as might be expected given higher atmospheric-moisture content and a deepening troposphere, will increase the frequency with which ARs penetrate inland across significant topographic barriers100. Consequently, inland regions such as the western USA are anticipated to have a greater availability of atmospheric moisture. Nevertheless, this inland penetration of atmospheric moisture does not guarantee higher precipitation, given dependence on air-mass saturation (more moisture is needed to achieve this in a warmer world) and the interactions between these air masses and dynamical mechanisms that force vertical ascent101.

The moistening of the atmosphere and the thermodynamic response of IVT to warming is, therefore, expected to increase precipitation related to ARs overall. Dynamic responses seem to have the largest effect on location, rather than on intensity. The poleward migration of ARs and potential modification of moisture-source regions will shift associated precipitation patterns.

Atmospheric river trends and projections

While physical theory has provided valuable insight into warming-related changes in ARs, the short duration of the satellite record and lack of observations over regions where they develop hinders the identification of trends in their behaviour. Evidence of change, therefore, exists in the form of regional case studies, trends in precipitation extremes and long-term reanalysis records.

Many studies have focused on understanding observed changes in ARs along the western coastline of North America, motivated by unprecedented hydroclimatic volatility over the last decade102. Here, AR activity has been increasing since 1948 (refs103,104), possibly linked to the warming of sea-surface temperatures in the western Pacific attributable to anthropogenic climate change105. For instance, a 20% increase in AR days has been observed in British Columbia106. In addition to increased activity, the temperatures of landfalling ARs to the US West Coast have risen since the 1980s, ranging between 0.69 and 1.65 °C over the entire region, depending on season and latitude60. Elsewhere, understanding of observed changes is extremely limited.

Global climate models (GCMs), however, offer an opportunity to understand projections of AR characteristics (including intensity, frequency and location) in a warming climate. GCMs are excellent tools to investigate the links between ARs and the large-scale circulation, and identify the thermodynamic processes involved throughout the lifetime of ARs. To date, most projection studies have relied on simulations from the Fifth Coupled Model Intercomparison Project (CMIP5), with a horizontal grid spacing of roughly 1.5–2.5° (150–250 km). This resolution is technically high enough to detect ARs but is too coarse to capture the fine-scale features involved within ARs, including interactions with orography. An expanded discussion of the limitations of current simulations is found in Box 2.

Globally, a comparison between the historical (1979–2002) and future (2073–2096) periods identified a 50% increase in AR frequency of occurrence — of nearly equal magnitude in the northern and southern hemispheres107 (Fig. 2). Projections also reveal a total decrease in the total number of AR events but an increase in those events’ width and length in a future climate107. It should be noted, however, that those increases may be an artefact of the increases in IVT with warming.

Fig. 2: Projected changes and impacts in atmospheric rivers.

Summary schematic of the main changes to atmospheric-river (AR) characteristics and impacts under warming. Red and blue symbols reveal increases and decreases, respectively; for frequency, red refers to a poleward movement and blue an equatorward movement of landfall. Light red and blue symbols with ‘?’ indicate uncertainty in the projection. Grey symbols indicate unknown changes. Background shading illustrating AR frequency increases is based on Espinoza et al.107.

Many studies also use GCMs to examine the regional characteristics of ARs in a warming climate11,34,52,64,66,88,108,109,110,111,112,113. In Europe, for example, the number of AR days is anticipated to increase by 127–275% under RCP 8.5 (ref.64) when comparing 1974–2004 to 2070–2099. Similarly, along the western coast of the USA, the frequency of IVT days above the historical 99th percentile is projected to increase by up to 290% over the same time period113, consistent with the projected increases shown elsewhere109,110. A summary of these regional changes is shown in Fig. 2 and Table 1, revealing the high degree of uncertainty or absent information outside of the western coastlines of North America and Europe.

Table 1 Summary of atmospheric river responses to warming

Figure 3 shows a comparison of thermodynamic (left column) and dynamic (right column) responses of IVT to warming. The calculations use data from a high-resolution data set of historical simulations and RCP 8.5 projections of the end of the 21st century. The panels show the dominance of thermodynamic changes over those from dynamics, in line with results from the UK and the western coastline of North America64,65,108,110,113.

Fig. 3: Decomposition of integrated vapour transport.

Thermodynamic (left column) and dynamic (right column) responses to warming for the West Pacific (part a), Australasia (part b), South Pacific (part c), North Pacific (part d), North Atlantic (part e) and South Atlantic (part f). The panels show the average response over all available Atmospheric River Tracking Method Intercomparison Project (ARTMIP) catalogues that participated in the Tier 2 project based on high-resolution (0.25°, 3-hourly) climate-change simulations from the International CLIVAR C20C+ Detection and Attribution project176. A full list of algorithms included in this figure can be found in the supplementary material. Stippling in the right column indicates agreement in the sign of the change between 80% of algorithms. There is no disagreement in the sign of the change in the thermodynamic response, so stippling is not shown in the left column. The historical climatology of integrated vapour transport (IVT) for landfalling atmospheric rivers is illustrated in black contours (contours starting at 200 kg m−1 s−1 and increasing in intervals of 50). The decomposition methodology follows that of ref.64, in which IVT is rescaled so that the left column shows the change in moisture between Representative Concentration Pathway 8.5 (RCP 8.5) and the historical period, and the right column shows the change in winds between RCP 8.5 and the historical period.

Also revealed, however, is the uncertainty in diagnosing dynamical responses due to biases in the mean position of the jet in the CMIP5 models64. As discussed previously, dynamical changes are most discernible at lower latitudes, where the projected expansion of the subtropics and the poleward shift of the jet have the most influence. For example, in Mediterranean climate zones of the lower mid-latitudes, poleward shifts in the storm track are projected to also shift the distribution of AR landfalls, resulting in a decrease in both the amount and frequency of winter precipitation66,114,115. One exception is California, where many GCMs predict a southward migration of the mid-winter storm track caused by an El Niño-like shift in climatological sea-surface temperatures108,110. This effect is partly compensated in the annual mean by poleward storm-track changes in the spring and fall64. Significantly, even in most of the Mediterranean climates that are affected by storm-track shifts, the strongest ARs are still projected to intensify at roughly the Clausius–Clapeyron rate expected from thermodynamics alone114. Combined with a decrease in total precipitation in these regions, this result implies a substantial increase in precipitation volatility, characterized by an increase in the frequency of both wet and dry extremes108,110,114,116. In addition to an increase in subseasonal variability, CMIP5 models projected a sharpening of the seasonal cycle of AR frequency in California that contributes to a sharpening of the seasonal cycle of extreme precipitation in the region, with important implications for floods and fire hazards117.

Impacts of atmospheric rivers on land

Hydrological impacts

The interaction of topography with the intense moisture transport found in ARs generally tie them to substantial hydrological impacts when they make landfall. These impacts are primarily felt through influences on water resources and through precipitation-related hazards, such as floods and landslides. Indeed, ARs have both beneficial and destructive characteristics, as indicated by a recently developed AR scale that quantifies the transition from beneficial precipitation and fewer hazards (AR categories 1–2) to heavy precipitation and numerous hazards (AR categories 4–5)54. Here, we discuss the observed hydrological impacts of ARs.

On the global scale, ARs contribute approximately 22% of the global run-off, reaching 50% in certain regions118. The western coast of the USA is one such region, where the visibility of AR impacts has resulted in a wealth of hazard-related literature summarized in Fig. 2 and Table 1. Here, ARs are associated with numerous wintertime extreme-precipitation events, which, in turn, have been connected to riverine flooding. For instance, ARs have been found to control the upper tail of peak flood-frequency distribution119 and account for 80–90+% of the annual maximum peak discharge in 1,375 long-term stream gauges120. In the Russian River, northern California, all seven floods that exceeded the monitor stage between 1997 and 2006 were further linked to ARs121, as were 46 of 58 annual maximum flood peaks in four basins in western Washington122. The impacts of ARs are not limited to riverine flooding; 40–60% of annual sea-level maxima at several sites along the West Coast were also connected to AR storm events123.

The effects of ARs also extend beyond the western coast of the USA, albeit with decreasing (yet hydrologically important) magnitudes. For example, in semi-arid north-eastern Arizona, ARs dominate heavy precipitation events, explaining 64–72% of precipitation exceeding the 98th percentile. This excess rainfall contributes to rain-on-snow events, increased run-off and 45% of annual maximum flows to inland basins124. Over the central part of the USA, ARs are further found to account for 20–70% of the heaviest daily precipitation extremes and more than 70% of flood events125, including catastrophic floods in the Midwest in June 2009 (ref.126) and in Tennessee in May 2010 (ref.127). In the south-east, as much as 41% of non-summer heavy-precipitation events (above 100 mm day −1) are connected to ARs41. In addition to precipitation impacts, hazards related to ARs also manifest in damaging winds, with the majority of insurance losses in excess of 1 billion USD linked to ARs23.

ARs are further associated with precipitation extremes over much of western Europe, where observations show the importance of topography for driving precipitation from landfalling events22. Compared with what is observed in the western USA, AR-related impacts reach far inland in western Europe. Broadly, ARs contribute up to 30% of precipitation, but exact distributions are sensitive to seasonal variability22. Over the UK, ARs are a dominant contributor to wintertime precipitation extremes (50% compared with only 20% in the summer months) and floods32. In a study of nine different river basins, for example, 40–80% of flood events were associated with persistent ARs33. Similarly, over Norway, ARs contribute 56 of 58 of the most extreme daily-precipitation events128 and also tied to costly flood events over that region31. Over the Iberian Peninsula, the association with ARs is more nuanced, with a clear zonal gradient in the importance of their landfall to precipitation extremes35; some studies indicate a weak relationship between summertime precipitation extremes and ARs17, whereas others reveal that ARs still play a significant role in the summertime, at least in Portugal, explaining 9 of 10 precipitation extremes between 1950 and 2007 (ref.129).

Elsewhere, the influence of ARs has been studied comparatively less. However, evidence suggests that 80% of days with heavy precipitation conditions (46 days total) over the central Andes are attributable to AR conditions26. Here, AR events are distinguished from other precipitation-producing phenomena by an increase in the intensity of moist upslope flow, producing rainfall accumulations that are more than twice those for non-AR conditions27,28. South African wintertime precipitation has been further linked to persistent AR activity, with approximately 70% of the top 50 daily-precipitation extremes experienced during AR events29. ARs have also been documented to impact the hydrology of East Asia; ARs account for between 14% and 44% of precipitation falling during the extended summer over Taiwan, southern China, the Korean Peninsula, and central and western portions of Japan25.

ARs frequently contribute to compound events (the combination of multiple climate drivers that contribute to societal or environmental risks and which may increase in the future130), particularly when heavy precipitation occurs together with or in close succession to other natural hazards. Specifically related to ARs are their ties to precipitation extremes and warm, moist air. For example, in October 2011 in the Bernese Alps of Switzerland, the combined effect of a heavy snowfall event followed by the passage of an AR resulted in a rapid increase of temperatures and melting of snowpack131. The resultant flooding of the valley below had costly impacts on the infrastructure and security of that region. In California, several studies have connected post-fire debris flows132 and landslides133 to the incidence of landfalling ARs, either in their interaction with water-resistant wildfire burn scars or by saturation of the soil. The potential for secondary hazards that outweigh the initial impact of ARs is also possible.

Despite the hazardous effects of ARs, they can also be beneficial by providing precipitation that is essential for water supply and resources52. Over the west coast of the USA, for example, ARs are thought to provide an average of 30–50% of annual precipitation52,90 and have been responsible for ending 33–74% of droughts in the region134, including the persistent California drought from 2012 to 2016 (ref.135). Indeed, it has been determined that, in regions currently frequented by ARs, the recurrence of droughts would increase by up to 90% in the absence of ARs118, due to both the immediate precipitation responses and the longer-term persistence of soil moisture after the event itself136.

ARs are significant contributors to the snowpack, and, hence, water resources in regions where snow makes up a substantial fraction of the water supply year-round. For example, ARs contribute between 30–40% of the total season accumulation of snow water equivalent (SWE) across the Sierra Nevada90. Unlike non-AR events that build the snowpack over multiple storms throughout the cold season, as few as 1–2 extreme AR-related snowfall events dominate contributions to SWE in the Sierra Nevada. In contrast, ARs making landfall in the US Pacific Northwest produce average gains in SWE given topographical differences and a subsequent larger fraction of rain30.

Because of their warmer temperatures, ARs disproportionately contribute to rain-on-snow events that increase the ratio of streamflow to precipitation137,138. In general, snowpack ablates more during AR than non-AR events because of the higher temperatures, but increased long-wave radiation also plays a secondary role139. The importance of rain-on-snow events in contributing to run-off is demonstrated by the significant increase of the run-off-to-precipitation ratio with (74%) and without (43%) pre-existing snowpack during AR landfall in the western USA139. Overall in the western USA, ARs explain 30–60% of the variability of annual run-off and sharpen the seasonality of water-resources availability in the west coast mountain watersheds by reducing the fraction of winter precipitation that accumulates as snowpack on April 1st139. In Europe, by contrast, rain-on-snow events are not as well documented. Nevertheless, limited case studies exist, such as in the Bernese Alps, Switzerland, where an AR event on 10 October 2011 caused substantial damage due to flooding131.

Trends in projected impacts

Given the substantial hydrological impacts of ARs in the present climate, and the projected changes in AR characteristics expected in the future, in this section, we outline how precipitation processes and impacts may also change. In many mountainous regions influenced by landfalling ARs, warming is expected to alter hydrological regimes and water resources. Increases in the ratio of rainfall to snowfall during the wet season will increase the likelihood of wintertime flooding140. With warmer temperatures, the timing of the peak snowmelt occurs earlier in the cold season, which has the effect of reducing streamflow in late spring or early summer141,142,143. Contraction of the snowmelt season towards winter and early spring reduces the energy available for melt, which can lead to a reduction in the snowmelt rate, with potential implications for streamflow, soil moisture and ecosystems144.

Climate change may further exacerbate the impacts of AR storms on the snowpack and rain-on-snow events. However, the visibility of any trends is highly dependent on climatological temperatures145, which, in turn, depend on the surface elevation. This nuance is apparent in high-resolution regional-climate simulations, which project less frequent rain on snow at lower elevations (a decrease of between 2 and 20 days year−1), but the opposite at higher elevations (an increase of between 2 and 10 days year−1) in the western USA146. At lower elevations, similar projections show a decline in the snowpack, which reduces the chance of the coexistence of rainfall and snow146. However, warming has less of an effect on snowpack at higher elevations, while a shift from snowfall to rainfall may enhance the chance of rain on snow. These same simulations also indicate an increase of flood risk between 20% and 200%, with the most considerable changes found in high-altitude mountains, including the Sierra Nevada, the Colorado River headwaters and the Canadian Rocky Mountains. It should be noted that the studies reviewed here do not isolate AR-induced versus non-AR-induced changes. However, the fact that rain-on-snow events happen more under AR conditions suggests that the projected changes in rain on snow are relevant. These results motivate a more in-depth analysis of changes in snowpack, rain on snow and flooding in the future.

The winter of 2016–2017 was an extremely wet year in California, with record extreme precipitation associated with an abnormally high number of intense ARs making landfall57. Probing the hydrological conditions of this wet year with and without historical and future warming, land-surface-model simulations show that historical warming has already reduced the Sierra Nevada SWE by 20% and increased early-season run-off by 30%147. Snowpack loss will continue under future warming, resulting in a more extreme run-off related to a smaller snow-to-rain ratio, rather than to increased snowmelt144,146. Altogether, historical warming has already exacerbated extreme run-off in the Sierra Nevada in the above-normal AR winter of 2016–2017 (ref.57). Under future warming, similar winter conditions suggest an even larger increase in flood risk.

Investigations of projected impacts specific to ARs are scarce but are consistent with the more general review summarized above. British Colombia’s Fraser River is an example of a mid-latitude basin influenced by nearby topography and by ARs. By the end of the 21st century under RCP 8.5, peak flow in this basin is increasingly decoupled from springtime snowmelt due to the decline in winter snowpack, and, instead, coupled to AR-related precipitation extremes148. Further work suggests that the increased frequency and intensity of projected ARs affecting this basin manifests as more frequent and larger wintertime flows, and an increase in the likelihood of flooding149. Similar results were found on the Salt River and Verde River basins in Arizona150. Compared with the present, ARs affecting middle and high elevations in the Pacific Northwest are expected to result in more liquid than solid precipitation, potentially exacerbating the flood risk100.

Summary and future perspectives

In this Review, we have identified key AR characteristics that are likely to change with anthropogenic warming. Our focus here has been to connect ongoing theoretical research on precipitation extremes with knowledge of ARs. Within a theoretical framework, future ARs are expected to carry more moisture, though moisture increases do not necessarily translate to increases in moisture transport, as storm-track changes and jet shifts also play a role. Areas with elevated terrain are most susceptible to increases in precipitation extremes attributable to ARs; however, in the absence of topography, effects are expected to scale in line with Clausius–Clapeyron61 and thermodynamic responses (Fig. 2). Projections further reveal increases in frequency and a general poleward shift in landfall location. When combined with enhanced atmospheric moisture and warmer temperature, the hydrological impacts of ARs may also be exacerbated (Fig. 3).

Despite a strong theoretical basis for understanding AR projections in the future, simulations of sufficient resolution to represent AR processes remain limited. Circulation drivers that modulate AR landfall location and duration, for example, are vital to understanding AR impacts on land151, but are a key source of uncertainty. Dynamic contributions to changes in IVT are much smaller, but may increase in importance in the transition regions between the expanding subtropics and the mid-latitudes. Uncertainty in projecting changes in the transition regions is strongly tied to uncertainty in projecting changes in tropical circulation and high-latitude processes, pointing to the fundamental challenge in modelling convection and cryosphere processes, respectively, in Earth-system models.

Given their importance to water resources, the ability to forecast AR impacts at extended ranges is essential, especially when factoring in the relatively long timescales needed for resource mobilization. Regions that rely on ARs for the replenishment of reservoirs and snowpack can feel their absence just as much as their presence. However, questions remain about the processes that contribute to their evolution before landfall, limiting forecasting capabilities. Thus, increased understanding of such processes — including diabatic effects of ARs on downstream weather-system development17 — is rapidly needed to improve prediction and, thereby, water-resource management. It is well known that current models do not accurately represent the effects of latent-heat release83. Given the projected increases in atmospheric moisture and, therefore, in IVT related to ARs, there is an urgent need to better understand how they interact with large-scale circulation. This insight is particularly relevant in understanding the interactive feedbacks between ARs and cyclone intensification83, which have implications on their precipitation signatures on land.

Although ARs are beneficial water resources, they can also have devastating and costly effects on human populations. An emerging area of research focuses on the intersection between the physical and human-related impacts associated with ARs. In the US West Coast, for example, flood damages linked to even a small increase in AR intensity can translate to large economic losses152. The interrelation between human activities, such as expansion of human development153 and modification of surface processes, means that new approaches are needed to communicate AR impacts. Model frameworks that bridge physical impacts with economic costs and policy development can be useful in this regard154. Similar approaches are needed to pass scientific understanding to stakeholders, such as water managers and policymakers, especially for weather extremes that are projected to worsen in the future.

AR characteristics over the North Pacific and impacts to the US West Coast serve as a test bed for the development of our knowledge of their impacts and variability. Figure 3 reveals robust understanding of the changes and impacts in this region, but an absence of understanding or high degree of uncertainty elsewhere. For instance, South America, South Africa and East Asia are strongly impacted by ARs, but our knowledge here is highly constrained by inadequate observational networks or field campaign data, as well as lack of model validation. Exploration of ARs at the global scale, therefore, represents the next frontier, including the high latitudes where analysis is urgently needed, given links to surface melt and glacial mass balance. Global and region-specific catalogues from the many ARTMIP subprojects represent an excellent resource for this work.


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L.R.L. and C.A.S. (NCAR via NSF IA 1947282) are supported by the U.S. Department of Energy Office of Science Biological and Environmental Research as part of the Earth and Environmental System Modeling Regional and Global Model Analysis program area. Pacific Northwest National Laboratory is operated for the Department of Energy by Battelle Memorial Institute under contract DE-AC05-75RL01830. The National Center for Atmospheric Research (NCAR) is sponsored by the National Science Foundation (NSF) under Cooperative Agreement 1852977. G.V. is supported by the U.S. Army Corps of Engineers’ Institute for Water Resources. A.M.R. is supported by the Scientific Employment Stimulus 2017 from FCT (CEECIND/00027/2017). Atmospheric River Tracking Method Intercomparison Project (ARTMIP) is a grass-roots community effort and has received support from the U.S. Department of Energy Office of Science Biological and Environmental Research as part of the Regional and Global Climate Modeling Program, and the Center for Western Weather and Water Extremes at Scripps Institute for Oceanography at the University of California, San Diego.

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The authors all contributed equally to the identification of main topics and their organization in the article. A. E. Payne led the writing and revision of the manuscript, with input and contributions from N. Siler (theory), L. R. Leung (theory, impacts), A. M. Ramos (projections), G. Villarini (impacts), C. A. Shields (Box 1) and M.-E. Demory (Box 2). A. E. Payne directed the modification of Fig. 1 and designed Figs. 2 and 3. C. A. Shields contributed the figure in Box 1 and M.-E. Demory contributed the figure in Box 2.

Correspondence to Ashley E. Payne.

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Nature Reviews Earth & Environment thanks Y. Kamae, F. Dominguez, V. Espinoza and M. Nayak for their contribution to the peer review of this work.

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Payne, A.E., Demory, M., Leung, L.R. et al. Responses and impacts of atmospheric rivers to climate change. Nat Rev Earth Environ 1, 143–157 (2020).

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