Report

Model Projections of an Imminent Transition to a More Arid Climate in Southwestern North America

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Science  25 May 2007:
Vol. 316, Issue 5828, pp. 1181-1184
DOI: 10.1126/science.1139601

Abstract

How anthropogenic climate change will affect hydroclimate in the arid regions of southwestern North America has implications for the allocation of water resources and the course of regional development. Here we show that there is a broad consensus among climate models that this region will dry in the 21st century and that the transition to a more arid climate should already be under way. If these models are correct, the levels of aridity of the recent multiyear drought or the Dust Bowl and the 1950s droughts will become the new climatology of the American Southwest within a time frame of years to decades.

The Third Assessment Report of the Intergovernmental Panel on Climate Change (IPCC) reported that the average of all the participating models showed a general decrease in rainfall in the subtropics during the 21st century, although there was also considerable disagreement among the models (1). Subtropical drying accompanying rising CO2 was also found in the models participating in the second Coupled Model Intercomparison Project (2). We examined future subtropical drying by analyzing the time history of precipitation in 19 climate models participating in the Fourth Assessment Report (AR4) of the IPCC (3). The future climate projections followed the A1B emissions scenario (4), in which CO2 emissions increase until about 2050 and decrease modestly thereafter, leading to a CO2 concentration of 720 parts per million in 2100. We also analyzed the simulations by these models for the 1860–2000 period, in which the models were forced by the known history of trace gases and estimated changes in solar irradiance, volcanic and anthropogenic aerosols, and land use (with some variation among the models). These simulations provided initial conditions for the 21st-century climate projections. For each model, climatologies were computed for the 1950–2000 period by averaging over all the simulations available for each model. All climate changes shown here are departures from this climatology.

We define an area (shown as a box in Fig. 4A) called “the Southwest” (including all land between 125°W and 95°W and 25°N and 40°N) that incorporates the southwestern United States and parts of northern Mexico. Figure 1 shows the modeled history and future of the annual mean precipitation minus the evaporation (PE), averaged over this region for the period common to all of the models (1900–2098). The median, 25th, and 75th percentiles of the model PE distribution and the median of P and E are shown. For cases in which there were multiple simulations with a single model, data from these simulations were averaged together before computing the distribution. PE equals the moisture convergence by the atmospheric flow and (over land) the amount of water that goes into runoff.

Fig. 1.

Modeled changes in annual mean precipitation minus evaporation over the American Southwest (125°W to 95°W and 25°N to 40°N, land areas only), averaged over ensemble members for each of the 19 models. The historical period used known and estimated climate forcings, and the projections used the SResA1B emissions scenario. The median (red line) and 25th and 75th percentiles (pink shading) of the PE distribution among the 19 models are shown, as are the ensemble medians of P (blue line) and E (green line) for the period common to all models (1900–2098). Anomalies (Anom) for each model are relative to that model's climatology from 1950–2000. Results have been 6-year low-pass Butterworth-filtered to emphasize low-frequency variability that is of most consequence for water resources. The model ensemble mean PE in this region is around 0.3 mm/day.

In the multimodel ensemble mean, there is a transition to a sustained drier climate that begins in the late 20th and early 21st centuries. In the ensemble mean, both P and E decrease, but the former decreases by a larger amount. PE is primarily reduced in winter, when P decreases and E is unchanged or modestly increased, whereas in summer, both P and E decrease. The annual mean reduction in P for this region, calculated from rain gauge data within the Global Historical Climatology Network, was 0.09 mm/day between 1932 and 1939 (the Dust Bowl drought) and 0.13 mm/day between 1948 and 1957 (the 1950s Southwest drought). The ensemble median reduction in P that drives the reduction in PE reaches 0.1 mm/day in midcentury, and one quarter of the models reach this amount in the early part of the current century.

The annual mean PE difference between 20-year periods in the 21st century and the 1950–2000 climatology for the 19 models are shown in Fig. 2. Almost all models have a drying trend in the American Southwest, and they consistently become drier throughout the century. Only 1 of the 19 models has a trend toward a wetter climate. Of the total of 49 individual projections conducted with the 19 models, even as early as the 2021–2040 period, only 3 projections show a shift to a wetter climate. Examples of modeled history and future precipitation for single simulations of four individual models are shown in Fig. 3 and provide an idea of potential trajectories toward the more arid climate.

Fig. 2.

The change in annual mean PE over the American Southwest (125°W to 95°W and 25°N to 40°N, land areas only) for 19 models (listed at left), relative to model climatologies from 1950–2000. Results are averaged over 20-year segments of the current century. The number of ensemble members for each projection is listed by the model name at left. Black dots represent ensemble members (where available), and red dots represent the ensemble mean for each model.

Fig. 3.

The change in annual mean PE over the American Southwest (125°W to 95°W and 25°N to 40°N, land areas only) for four coupled models, relative to model ensemblemean climatologies from 1950–2000. The results are from individual simulations of the 1860–2000 period, forced by known and estimated climate forcings and individual projections of future climate with the SResA1B scenarios of climate forcings. Because the modeled anomalies have not been averaged together here, these time series provide an idea of plausible evolutions of Southwest climate toward a more arid state. The models are the National Center for Atmospheric Research Community Climate System Model (CCSM), GFDL model CM2.1, Max Planck Institut Für Meteorologie model ECHAM5, and Hadley Centre for Climate Change model HadCM3. All time series are for annual mean data, and a 6-year low-pass Butterworth filter has been applied.

The contours in Fig. 4, A to C, show a map of the change in PE for the decades between 2021 and 2040 minus those in the 1950–2000 period for one of the IPCC models: the Geophysical Fluid Dynamics Laboratory (GFDL) climate model CM2.1 (5). In general, large regions of the relatively dry subtropics dry further, whereas wetter, higher-latitude regions become wetter still. In addition to the American Southwest, the southern Europe–Mediterranean–Middle East region also experiences a severe drying. This pattern of subtropical drying and moistening at higher latitudes is a robust feature of current projections with different models of future climate (6).

Fig. 4.

The change in annual means of PE for the 2021–2040 period minus the 1950–2000 period [contours in (A) to (C)] and contributions to the change in vertically integrated moisture convergence (colors; negative values imply increased moisture divergence) by the mean flow, due to (A) changes in the flow, (B) the specific humidity, and (C) the transient-eddy moisture convergence, all for the GFDL CM2.1 model. The box in (A) shows the area we defined as “the Southwest.”

The change (δ) in PE (in meters per second) is balanced by a change in atmospheric moisture convergence, namely Embedded Image(1)

Overbars indicate monthly means, primes represent departures from the monthly mean, ρw is the density of water, g indicates the acceleration due to gravity, and ∇ indicates the horizontal divergence operator. The change in moisture convergence can be divided into contributions from the mean flow and from eddies. In the former, the atmospheric flow Embedded Image and the moisture () are over a month before computing the moisture transport, whereas the latter is primarily associated with the highly variable wind (u′) and moisture (q′) fields within storm systems. The moisture convergence is integrated over the pressure (p) from the top of the atmosphere (p = 0) to the surface (ps). The mean wind and humidity fields in Eq. 1 can be taken to be their climatological fields. (The rectification of interannual variability in the monthly mean flow and moisture fields is found to be negligible.) Changes in the mean flow contribution can, in turn, be approximated by one part associated with the climatological circulation from 1950 to 2000 Embedded Image, operating on the increase in climatological atmospheric humidity (δ, a consequence of atmospheric warming), and by another part due to the change in circulation climatology Embedded Image, operating on the atmospheric humidity climatology from 1950 to 2000 Embedded Image. The nonlinear term involving changes in both the mean flow and the moisture field is found to be relatively small. Hence, Eq. 1 can be approximated by: Embedded Image(2) Embedded Image We therefore think in terms of a threefold decomposition of PE, as displayed in Fig. 4 (colors) for the GFDL CM2.1 model: (i) a contribution from the change in mean circulation, (ii) a contribution from the change in mean humidity, and (iii) a contribution from eddies.

The mean flow convergence term involving only changes in humidity (Fig. 4B) causes increasing PE in regions of low-level mean mass convergence and decreasing PE in regions of low-level mean mass divergence, generally intensifying the existing pattern of PE (6). This term helps to explain much of the reduction in PE over the subtropical oceans, where there is strong evaporation, atmospheric moisture divergence, and low precipitation (6). Over land areas in general, there is no infinite surface-water source, and PE has to be positive and sustained by atmospheric moisture convergence. Over the American Southwest, in the current climate, it is the time-varying flow that sustains most of the positive PE, whereas the mean flow diverges moisture away. Here, the “humidity contribution” leads to reduced PE, as the moisture divergence by the mean flow increases with rising humidity. Over the Mediterranean region, there is mean moisture divergence, and rising humidity again leads to increased mean moisture divergence and reduced PE.

Over the ocean, the contribution of humidity changes to changes in PE can be closely approximated by assuming that the relative humidity remains fixed at its 1950–2000 values (6). Over almost all land areas and especially over those that have reduced PE, the relative humidity decreases in the early 21st century. This is because, unlike over the ocean, evaporation cannot keep pace with the rising saturation humidity of the warming atmosphere. Over land, the humidity contribution to the change in PE is distinct from that associated with fixed relative humidity.

Decreases in PE can also be sustained by changes in atmospheric circulation that alter the mean moisture convergence, even in the absence of changes in humidity (Fig. 4A). This “mean circulation contribution” leads to reduced PE at the northern edge of the subtropics (e.g., the Mediterranean region, the Pacific and the Atlantic around 30°N, and parts of southwestern North America). The change in moisture convergence by the transient eddies (Fig. 4C) dries southern Europe and the subtropical Atlantic and moistens the higher-latitude Atlantic, but it does not have a coherent and large impact over North America.

A substantial portion of the mean circulation contribution, especially in winter, can be accounted for by the change in zonal mean flow alone (not shown in the figures), indicating that changes in the Hadley Cell and the extratropical mean meridional circulation are important. Increases in humidity and mean moisture divergence, changes in atmospheric circulation, and the intensification of eddy moisture divergence cause drying in the subtropics, including the area over western North America and the Mediterranean region. For the Southwest region, the annual mean PE decreases by 0.086 mm/day, which is largely accounted for by an increase in the mean flow moisture divergence. Changes in the circulation alone contribute 0.095 mm/day of drying, and changes in the humidity alone contribute 0.032 mm/day. These changes are modestly offset by an increased transient-eddy moisture convergence of 0.019 mm/day. (7).

Within models, the poleward edge of the Hadley Cell and the mid-latitude westerlies move poleward during the 21st century (810). The descending branch of the Hadley Cell causes aridity, and hence the subtropical dry zones expand poleward. In models, a poleward circulation shift can be forced by rising tropical sea surface temperatures (SSTs) in the Indo-Pacific region (11) and by uniform surface warming (12). The latter results are relevant because the spatial pattern of surface warming in the AR4 models is quite uniform away from the poles. One explanation (13, 14) is that rising tropospheric static stability, an established consequence of moist thermodynamics, stabilizes the subtropical jet streams at the poleward flank of the Hadley Cell against baroclinic instability. Consequently, the Hadley Cell extends poleward (increasing the vertical wind shear at its edge) to a new latitude where the shear successfully compensates for the suppression of baroclinic instability by rising static stability.

Although increasing stability is likely to be a substantial component of the final explanation, a fully satisfying theory for the poleward shift of the zonal mean atmospheric circulation in a warming world must account for the complex interplay between the mean circulation (Hadley Cell and the mid-latitude Ferrell Cell) and the transient eddies (13, 14) that will determine where precipitation will increase and decrease in the future. However, not all of the subtropical drying in the Southwest and Mediterranean regions can be accounted for by zonally symmetric processes, and a full explanation will require attention to moisture transport within localized storm tracks and stationary waves.

The six severe multiyear droughts that have struck western North America in the instrumental record have all been attributed (by the use of climate models) to variations in SSTs in the tropics, particularly persistent La Niña–like SSTs in the tropical Pacific Ocean (1519). The projected future climate of intensified aridity in the Southwest is caused by different processes, because the models vary in their tropical SST response to anthropogenic forcing. Instead, it is caused by rising humidity that causes increased moisture divergence and changes in atmospheric circulation cells that include a poleward expansion of the subtropical dry zones. The drying of subtropical land areas that, according to the models, is imminent or already under way is unlike any climate state we have seen in the instrumental record. It is also distinct from the multidecadal megadroughts that afflicted the American Southwest during Medieval times (2022), which have also been attributed to changes in tropical SSTs (18, 23). The most severe future droughts will still occur during persistent La Niña events, but they will be worse than any since the Medieval period, because the La Niña conditions will be perturbing a base state that is drier than any state experienced recently.

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