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Anthropogenic and Natural Influences in the Evolution of Lower Stratospheric Cooling

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Science  24 Feb 2006:
Vol. 311, Issue 5764, pp. 1138-1141
DOI: 10.1126/science.1122587

Abstract

Observations reveal that the substantial cooling of the global lower stratosphere over 1979–2003 occurred in two pronounced steplike transitions. These arose in the aftermath of two major volcanic eruptions, with each cooling transition being followed by a period of relatively steady temperatures. Climate model simulations indicate that the space-time structure of the observed cooling is largely attributable to the combined effect of changes in both anthropogenic factors (ozone depletion and increases in well-mixed greenhouse gases) and natural factors (solar irradiance variation and volcanic aerosols). The anthropogenic factors drove the overall cooling during the period, and the natural ones modulated the evolution of the cooling.

The global lower stratosphere—the region of the atmosphere from ∼12 to 22 km above the surface—has cooled substantially over the past two decades (15). The difference in temperature between 2000 and 1979 has been ascribed mainly to ozone depletion and increases in well-mixed greenhouse gases (4, 610). Observations indicate that the decrease in temperature was steplike rather than a steady decline (1, 3). Although the overall trend in temperature has been modeled previously (5, 9, 10), the steplike structure and the evolution of the cooling pattern in the observed global temperature time series has not been explained in terms of specific physical causes, whether these be external forcing and/or internal variability of the climate system. Thus, attribution of the unusual cooling features observed during the 1980s and 1990s has yet to be addressed, along with potential implications for the future.

We used a coupled atmosphere-ocean model (1113) to demonstrate that the complex space-time pattern of the lower stratospheric temperature anomalies is a consequence of the combined temporal changes in natural forcings [solar irradiance (14) and volcanic aerosols (15)] and anthropogenic forcings [well-mixed greenhouse gases (16), stratospheric (17) and tropospheric ozone (18), tropospheric aerosols (18), and land use (13)].

We performed five separate experiments to investigate the contributions of different forcing mechanisms to changes in lower stratospheric temperature: (i) natural plus anthropogenic (AllForc), (ii) natural (Nat), (iii) well-mixed greenhouse gases (Wmgg), (iv) well-mixed greenhouse gases plus stratospheric and tropospheric ozone (WmggO3), and (v) anthropogenic (Anth; that is, WmggO3 plus tropospheric aerosols and land-use change). For each case, an ensemble of simulations was performed. Individual ensemble members started from different points of a long control simulation with a fixed preindustrial (1860) atmospheric composition and were then integrated from 1861 through 2003. There were five ensemble members for (i); (ii) to (v) comprised three members each, starting from the same initial conditions as three of the AllForc integrations. The observed lower stratospheric temperatures (1979–2003) were from measurements (referred to as T4) made by channel 4 of the Microwave Sounding Unit on the National Oceanic and Atmospheric Administration's satellites (19). Synthetic T4 values were computed from the simulated temperature profiles as described in (5). The observed and simulated T4 results are expressed as annual mean temperature anomalies, relative to their respective 1979–1981 averages.

The observed time evolution of the zonally and annually averaged T4 temperature anomalies (Fig. 1A) illustrates the transient warming in ∼1982–1984 and ∼1991–1993 after the El Chichon (1982) and Pinatubo (1991) volcanic eruptions. This warming resulted from the radiative effects of the stratospheric sulfate aerosols formed after the eruptions (4, 9, 10). After the decay of the volcanic aerosols (∼2 years after eruption), the warming ceased, and the lower stratosphere in the 50°N-50°S domain cooled substantially relative to the pre-eruption period. After the steplike transition in ∼1985, the observed T4 values were relatively stable until the Pinatubo eruption. The decay of the Pinatubo-related warming was followed by a second steplike cooling in T4 (∼1994), and the anomaly remained approximately steady thereafter. The signature of the quasi-biennial oscillation (QBO) in temperature, a natural mode of climate variation (20), was clearly manifested at the equator. There was large dynamical variability at high latitudes, especially in the Northern Hemisphere (4, 21).

Fig. 1 (left).

Zonally and annually averaged temporal evolution (1979–2003) of lower stratospheric temperature (T4) anomalies (relative to 1979–1981 averages). EQ, equator. (A) Satellite observations (19). (B) AllForc model simulated response to natural and anthropogenic forcings. Model results are altitude-weighted as in (5), using the T4 weighting function. Fig. 2 (right). Ensemble-mean simulated evolution (1979–2003) of the zonally and annually averaged temperature (T4) anomalies (relative to the respective 1979–1981 averages) for (A) Nat, (B) WmggO3, and (C) Anth forcing cases. Model results are altitude-weighted as in (5), using the T4 weighting function.

The AllForc simulation (Fig. 1B) captures the primary features of the observed T4 anomalies, including the El Chichon and Pinatubo warming anomalies; the two steplike cooling transitions; and the ensuing prolonged, quasi-steady periods (∼1985–1990 and ∼1994–2000). The simulated evolution is spatially more homogeneous and exhibits less cooling than do observations made in the 1980s; the widespread extent and increased cooling in the 1990s is broadly consistent with observations. As in the observations, the model shows both cooling and substantial dynamical variability poleward of 50° (4, 68). The model lacks a QBO and hence does not replicate the observed periodicity of T4 near the equator.

The simulated influences due to the key forcings are illustrated in Fig. 2. As expected, Nat shows a large stratospheric warming after El Chichon and Pinatubo, but no overall trend (Fig. 2A). In contrast, WmggO3 and Anth (Fig. 2 B and C), exhibit a progressive greenhouse gas–dominated cooling of the global stratosphere (410, 22), with more cooling in the 1990s than in the 1980s. Anth generally has less cooling than WmggO3 at low latitudes. This difference is essentially due to solar warming by anthropogenic upper tropospheric aerosols in Anth (18, 23), with the effect implicitly sampled by the T4 weighting function (35). The increased cooling in AllForc (Fig. 1B) during ∼1994–2000 arises primarily from Anth (Fig. 2C), together with a smaller contribution from Nat (Fig. 2A). In contrast, during ∼1985–1990, Nat in some domains slightly offsets the Anth cooling (Fig. 2, A and C). Clearly, both Anth and Nat are needed to explain the AllForc evolution and to account for the observed space-time T4 pattern (Fig. 1A).

Figure 3A illustrates that the AllForc simulation successfully captures the complex observed time evolution of the global and annual mean T4 anomalies. The amplitudes of the observed and simulated cooling are very similar, both for the first “step” (1985–1990 minus 1979–1981; results are –0.40 and –0.38 K, respectively) and the second “step” (1994–2000 minus 1985–1990; results are –0.32 and –0.29 K, respectively). The model also replicates the relatively steady behavior of the observed T4 anomalies over ∼1994–2000 and the slight temperature increase between the late 1990s and 2003. These results enhance our confidence in the reliability of the model and the applied forcings. Externally forced changes in AllForc are large relative to the model's internally generated variability (Fig. 3A).

Fig. 3.

(A) Model-simulated ensemble-mean (AllForc, red curve) and Microwave Sounding Unit (MSU, black curve) satellite observations (19) of the globally and annually averaged temperature (T4) anomalies over 1979–2003 (relative to their respective 1979–1981 averages). The gray shading denotes the range of the five-member ensemble simulations and is a measure of the simulated internally generated variability of the climate system. (B) Model-simulated ensemble mean of the globally and annually averaged temperature (T4) anomalies (relative to the respective 1979–1981 averages) for the AllForc, Nat, Wmgg, WmggO3, and Anth radiative forcing cases, respectively.

In Fig. 3B, the comparison of WmggO3 and Wmgg shows that the overall lower stratospheric temperature decline is driven primarily by the depletion of ozone, and to a lesser extent by the increase in well-mixed greenhouse gases. Although the T4 Anth anomaly is less than WmggO3 because of the previously mentioned solar heating by anthropogenic aerosols in the upper tropsophere (see also Fig. 2, B and C), both exhibit a gradual increase of cooling until the mid- to late 1990s. In contrast, the global average Nat lacks an overall global mean cooling trend but contributes to the AllForc cooling in both decades and is comparable to Wmgg in specific nonvolcanic years.

In the first steplike cooling transition in ∼1985, the changes in well-mixed gases and ozone produce an increase in the cooling anomaly of Anth relative to the pre-eruption value (Figs. 2, B and C, and 3B). In contrast to Nat, there is a distinctly increasing cooling of Anth over 1985–1990 (Fig. 3B). During the ∼2-year presence of volcanic aerosols, the surface-troposphere system cools; after the aerosols decay, the surface and troposphere temperatures recover, but do so slowly owing to the thermal inertia of the oceans (9, 10, 24). The cooler surface and troposphere reduce the upwelling long-wave radiation flux, resulting initially in a slight cooling anomaly of the lower stratosphere in Nat. Added to this is the effect of solar cycle variations, yielding decreases in irradiance during the mid-1980s (1, 14). The net result is an approximately steady AllForc anomaly over ∼1985–1990 (Figs. 1B and 3B).

The second steplike cooling transition in ∼1994 is followed by another near-steady anomaly period (∼1994–2000; Fig. 3B). The sharp decline in Anth relative to the pre-eruption value is due to WmggO3 (Figs. 2, B and C, and 3B). In contrast to 1985–1990, stratospheric ozone depletion in the 1990s is easily the principal contributor to the Anth and AllForc cooling. This depletion levels off during the mid- to late 1990s, resulting in a near-flattening of the WmggO3 and Anth anomalies. After ∼1998, the cooling anomaly in WmggO3 decreases slightly, consistent with a lesser ozone depletion. The Nat cooling contribution again comprises a post–volcanic-aerosol cooling of the surface and troposphere as in the mid-1980s, plus the effect of another minimum in the solar cycle (14). In the mid-1990s, the Nat cooling (Fig. 2A), together with Anth (Fig. 2C), yields a substantial AllForc cooling (Figs. 1B and 3B). By the mid- to late 1990s, the Nat cooling contribution diminishes as the surface-troposphere system recovers from the volcanic cooling and the solar cycle proceeds to its next maximum (14). Thus, the deceleration of the AllForc cooling in the mid- to late 1990s (Figs. 1B and 3B) is traceable to stratospheric ozone changes coupled with natural influences.

The two steplike temperature transitions, followed by relatively steady periods (Figs. 1 and 3A), are thus a consequence of both anthropogenic and natural factors. The anthropogenic cooling influence becomes an important global feature by the late 1980s and a dominant one in the 1990s (Figs. 2, B and C, and 3B). Although the effect of volcanic aerosols on the transient warming in the lower stratosphere is known (4, 5, 9, 10), the results here show that natural forcing, despite lacking a trend, has contributed to the modulation of the 1979–2003 global cooling evolution. If the solar and volcanic aerosol forcing were entirely absent, the temperature evolution would have comprised a steady decrease driven by Anth, but this is inconsistent with the observations (Figs. 1A and 3B). The decadal-scale temperature decline that is dominated by stratospheric ozone depletion is very likely unprecedented in the historical evolution of the lower stratospheric thermal state. The juxtaposition of the 1979–2003 ozone loss, solar variation, and volcano effects in yielding the observed temperature evolution is also likely to be unusual.

In the 21st century, if ozone depletion were to continue unabated, the anthropogenic effects would outweigh natural forcing to an even greater extent than in the 1990s (Fig. 3B). The comparable value of the Nat cooling anomaly to that of Wmgg in years without volcanic aerosol influences (Fig. 3B) presents another implication for the future. With stratospheric ozone anticipated to recover over the next several decades because of a reduction in halogen loadings, and before the continued increase in well-mixed greenhouse gases enables them to be the dominant factor, natural forcing contributions to the global lower stratospheric temperature evolution could become relatively more important than in the period considered here.

An uncertainty in these quantitative estimates is the incomplete knowledge of the global vertical profile of ozone change immediately after volcanic eruptions (25, 26). Enhancements in global ozone loss due to volcanic aerosols, as indicated by chemical modeling (27) and not incorporated in the data set used here, could add to the simulated cooling. Including explicit stratospheric chemistry (28, 29) in future coupled atmosphere-ocean climate model simulations would provide further insights into the evolution of cooling. An increase in lower stratospheric water vapor will also contribute to a cooling (8, 30), although its space-time evolution is uncertain (31). Another uncertainty is the extent to which upper tropospheric species (such as aerosols) affect T4 temperatures. The observed variations in stratospheric ozone likely contain influences due to dynamical fluctuations, such as changes in planetary waves and stratosphere-troposphere coupling (1) and the perturbation of tropical stratospheric circulation due to volcanic aerosol heating (32). This suggests that internal system variations in ozone will affect global temperature changes, but probably much less than the large anthropogenic ozone loss over the period. Despite the uncertainties, the simulations described here quantitatively demonstrate the existence of an externally forced response in the observed 1979–2003 global lower stratospheric temperature time series, and they delineate the natural and anthropogenic influences on the evolution of the cooling.

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