Report

The Recent Increase in Atlantic Hurricane Activity: Causes and Implications

Science  20 Jul 2001:
Vol. 293, Issue 5529, pp. 474-479
DOI: 10.1126/science.1060040

This article has a correction. Please see:

Abstract

The years 1995 to 2000 experienced the highest level of North Atlantic hurricane activity in the reliable record. Compared with the generally low activity of the previous 24 years (1971 to 1994), the past 6 years have seen a doubling of overall activity for the whole basin, a 2.5-fold increase in major hurricanes (≥50 meters per second), and a fivefold increase in hurricanes affecting the Caribbean. The greater activity results from simultaneous increases in North Atlantic sea-surface temperatures and decreases in vertical wind shear. Because these changes exhibit a multidecadal time scale, the present high level of hurricane activity is likely to persist for an additional ∼10 to 40 years. The shift in climate calls for a reevaluation of preparedness and mitigation strategies.

During 1970–1987, the Atlantic basin experienced generally low levels of overall tropical cyclone activity. The relative lull was manifested in major hurricane (1) activity (Fig. 1), major hurricane landfalls on the East Coast of the United States and overall hurricane activity in the Caribbean. A brief resurgence of activity in 1988 and 1989 made it appear that the Atlantic basin was returning to higher levels of activity similar to the late 1920s through the 1960s (2). This notion was later discarded when the activity returned to lower levels from 1991–1994 (3), due in part to the long-lasting (1990–1995) El Niño event (4). This event ended in early 1995 and was followed later that year by one of the most active Atlantic hurricane seasons on record (5). Activity has been well above average each year since 1995, except for 1997. Here we address the question of whether or not the increase in activity reflects a long-term climate shift, as suggested by previous studies (6–9), and provide evidence that confirms this suggestion based on changes in oceanic and atmospheric conditions.

Figure 1

Number of major hurricanes from 1944 through 2000 (32). Less reliable data before routine aircraft reconnaissance dictate caution in the use of these data before 1944 (33). Solid horizontal reference line corresponds to sample mean (2.3). Dashed curved line is 5-year running mean. Also shown is the threshold of three major hurricanes per year (dashed straight line).

The North Atlantic basin (including the North Atlantic Ocean, the Caribbean Sea, and the Gulf of Mexico) exhibits substantial interannual and interdecadal variability of tropical cyclone activity. This variability is especially pronounced in major hurricane activity. Interdecadal major hurricane fluctuations occur in both landfall locations (10) and overall activity (11–13). Most of the deadliest and costliest Atlantic tropical cyclones (10) are major hurricanes. Major hurricanes account for just over 20% of the tropical storms and hurricanes that strike the United States but cause more than 80% of the damage (14).

Most Atlantic tropical cyclones form from atmospheric easterly (African) waves that propagate westward from Africa across the tropical North Atlantic and Caribbean Sea, primarily between 10° and 20°N [termed the “main development region” (MDR) (15,16) (see Fig. 2A)]. The Atlantic tropical cyclones not spawned by African waves usually form poleward of 25°N. African waves account for ∼60% of the Atlantic basin tropical storms and nonmajor hurricanes but ∼85% of major hurricanes (17). Almost all major hurricanes formed from African waves begin development (i.e., attain tropical depression status) in the MDR (15) and, thus, are more sensitive to climatic fluctuations in the tropics.

Figure 2

Atlantic sector of the first rotated EOF of non-ENSO global SST variability for 1870–2000 referred to as the “Atlantic multidecadal mode” (38, 39). (A) Spatial distribution of correlations between local monthly SST anomalies and the modal reconstruction over the indexed region (northern rectangle), the general area where the mode amplitude is the strongest. This distribution has a similar spatial structure to the actual rotated EOF and gives a measure of the local fractional variance (squared temporal correlation) accounted for at each grid point. Dashed lines give north and south boundaries of main development region (MDR) and box (10° to 14°N, 20° to 70°W) is region used to calculate data for Fig. 3. (B) Temporal reconstruction (annual means) of the mode-related variability averaged over the rectangular areain (A). Dashed curved lineis 5-year running mean. Although the signal is stronger in the North Atlantic, it is global in scope with positively correlated co-oscillations in parts of the North Pacific (55). For the multidecadal variations shown here, the coherence between the MDR and far North Atlantic is a robust feature. The SST fluctuations in the far North Atlantic could be used as a proxy for changes in the MDR.

Although the number of easterly waves in the tropical Atlantic is fairly constant from year to year, the fraction that develop into tropical cyclones varies substantially (18,19). The key to understanding the fluctuations on interannual and interdecadal scales is the MDR. The climatic forcing that affects that region can be separated into local and remote factors. In combination, these factors influence the number of waves that develop into tropical cyclones during each hurricane season. Local factors occur in the actual region and have a direct thermodynamic or dynamic connection to development. Remote factors occur away from the MDR, but are associated (via teleconnections) with conditions in that region. All factors vary on disparate temporal and spatial scales, and there is considerable interdependence between some of them. The extremely active 1995 season, for example, resulted from the juxtaposition of virtually all of the factors known to favor development (5). Among the local tropical Atlantic factors are the lower stratospheric Quasi-Biennial Oscillation (20,21), sea-level pressure (5, 20,22), lower tropospheric moisture (5), sea-surface temperature (SST) (23–25), and vertical shear of the horizontal environmental wind (15,26). The two local factors addressed here are SST and vertical shear.

In general, when looking for long-term variability, it is necessary to look at the oceans because their large thermal and mechanical inertia provide long-term memory and predictability (27). The oceans are the primary energy source for tropical cyclones. Localized SSTs play a direct role in providing moist enthalpy to power incipient tropical cyclones (5,25). Warmer SSTs decrease atmospheric stability, which increases the penetration depth of a vortex, thus, making developing tropical cyclones more resistant to vertical wind shear (28). Local SST greater than 26.5°C is usually considered to be a necessary condition for tropical cyclone development (26), and higher SST can increase overall activity (23–25). Multidecadal variations in major hurricane activity have been attributed to changes in the SST structure in the Atlantic (2, 12, 13) because tropical North Atlantic SSTs correlate positively with major hurricane activity. Although North Atlantic SSTs directly impact tropical cyclone activity as a local thermodynamic effect, it appears unlikely that this is their only physical link to hurricane activity. For influencing activity on interannual time scales, this local effect plays either a negligible role (for major hurricanes) or at best a secondary role (for all hurricanes) (24).

The dominant local factor for tropical cyclone activity is the magnitude of the vertical shear of the horizontal wind between the upper and lower troposphere, ∣Vz ∣. Strong Vz inhibits the formation and intensification of tropical cyclones [e.g., (15,26)], primarily by preventing the axisymmetric organization of deep convection. Local ∣Vz ∣ > ∼8 m s−1 is generally unfavorable for development (29). The climatological mean vertical wind shear,Vz , for August-September-October (ASO), the peak 3 months of the Atlantic hurricane season during which virtually all major hurricanes form, is westerly with a magnitude ∣Vz ∣ greater than 8 m s−1 over much of the basin (15,16). Climatologically high values for ∣Vz ∣ are one of the main reasons why conditions in the Atlantic basin are not especially conducive to tropical cyclone development. The tropical North Atlantic SST appears to act in concert with the overlying tropospheric circulation such that warmer SSTs correspond to reduced ∣Vz ∣ in the MDR (12, 24).

A key remote factor is SST variability in the central and eastern equatorial Pacific Ocean associated with El Niño–Southern Oscillation (ENSO). Positive Pacific SST anomalies associated with warm-phase ENSO (El Niño) have been linked to increased ∣Vz ∣ over the MDR, and conversely for cool-phase ENSO (La Niña) (15, 20,30). Another remote factor that has been linked to interannual and multidecadal variability in Atlantic basin tropical cyclone activity is rainfall variability over the western Sahel (2, 31), with positive rainfall anomalies associated with reduced ∣Vz ∣ over the MDR (15).

The most obvious indicator of a possible long-term shift are the changes in the tropical cyclone activity itself. The total number of tropical storms and nonmajor hurricanes in the North Atlantic basin has remained fairly constant from decade to decade (13). The numbers of major hurricanes and of Caribbean hurricanes, however, exhibit strong multidecadal variability. The late 1920s to the 1960s were very active, while both the 1900s through mid-1920s and the 1970s through the early 1990s were quiescent (2, 12,13).

The events of each year reflect a combination of temporal scales. Interannual fluctuations in activity occur in both high and low activity periods (Fig. 1). However, inhibitory influences during relatively inactive multidecadal periods set a limit on the possible level of activity. During 1944–1970 (the portion of the previous active multidecadal period shown in Fig. 1), the average number of major hurricanes per year was 2.7 (32–34). Six of the years produced four or more major hurricanes. In contrast, the average for the quieter period of approximately equal duration, 1971–1994, was only 1.5, with no years having more than three major hurricanes. The quieter period's threshold of three major hurricanes was then exceeded in 1995 for the first time since 1964. The average number of major hurricanes for 1995–2000 is 3.8 (34). Three of those years had four or more. The Net Tropical Cyclone activity (NTC) for the North Atlantic, another measure of activity (8), shows a similar combination of interannual and multidecadal fluctuations (35). The only year since 1995 with below average activity was 1997, when the Atlantic hurricane activity was suppressed by the strongest El Niño event of this century (36). Even with 1997 included, the mean number of major hurricanes and mean NTC for 1995–2000 are the highest of any consecutive 6 years in the 1944–2000 record. While this recent period spans only 6 years, it clearly belongs to a different low-frequency climate regime than the previous 24 years (1971–1994).

Studies of global SSTs using empirical orthogonal function (EOF) analysis [e.g., (37)] have shown that the primary source of interannual SST variability is the ENSO region. To analyze the relation of Atlantic tropical cyclone activity with Atlantic SST anomalies in a way that is independent of ENSO, it is helpful to first remove the teleconnected effects of ENSO on the Atlantic Ocean (38). The first rotated non-ENSO SST mode (39) represents interannual to multidecadal variability (Fig. 2). Because the mode's temporal variability is dominated by multidecadal-scale fluctuations (Fig. 2B) with the largest amplitudes in the Atlantic, we refer to it as the “Atlantic multidecadal mode.” The positive phase of the mode's spatial pattern (Fig. 2A) has warm SSTs in the tropical North Atlantic from 0° to 30°N (which includes the MDR) and in the far North Atlantic from 40° to 70°N. This mode is not local to the MDR; it is instead a large-scale feature that, because it is also present in the MDR, affects Atlantic tropical cyclone activity. The primary region for SST anomalies that would affect tropical cyclones directly would be in and just north of the MDR, i.e., ∼10° to 25°N (24, 40).

These multidecadal-scale fluctuations in SSTs closely follow the long-term fluctuations in Atlantic tropical cyclone activity (13). The time series for the Atlantic multidecadal mode (Fig. 2B), major hurricanes (Fig. 1) and NTC (35) all show similar multidecadal-scale shifts. Ignoring interannual fluctuations, major hurricane activity is high from 1944 through at least ∼1964 (Fig. 1), NTC is high through ∼1969 (35) and the Atlantic multidecadal mode is predominately warm until ∼1970 (Fig. 2B). Then, major hurricane activity and NTC are mostly below average and the Atlantic multidecadal mode colder from the early 1970s through the early 1990s. All three quantities have increased dramatically since 1995. Note also that the two busiest periods in the 1970s and 1980s, 1979–1981 and 1988–1990 (35), coincide with two short warming periods, 1979–1981 and 1987–1990 (see Fig. 2B), indicating the possibility of significant relations on shorter (decadal) time scales. The correlations between the 5-year running mean of the Atlantic multidecadal mode with the major hurricane and NTC running means are 0.72 and 0.81, respectively (41).

It has been hypothesized that multidecadal changes in oceanic temperatures, major hurricane activity and Sahel rainfall are related to fluctuations in the intensity of the thermohaline circulation in the North Atlantic (12, 42). A faster thermohaline circulation is suggested to be associated with warmer SSTs in the North Atlantic and colder SSTs in the South Atlantic. These conditions would enhance Sahel rainfall and decrease ∣Vz ∣ in the MDR. In other words, the decadal-scale SST fluctuations affecting Atlantic hurricane (particularly major hurricane) activity would likely produce the connection via changes in the upper- and lower-level zonal atmospheric circulations over the MDR (40). It is also possible, but less likely, that the changes in atmospheric circulation are forcing the SST changes. However, it is doubtful that long-term increased tropical cyclone activity could cause warmer North Atlantic SSTs since hurricanes result in a cooling of SSTs through vertical mixing and upwelling (e.g., 43).

Figure 3 shows the fluctuations in ∣Vz ∣ averaged for ASO for the south-central portion of the MDR where the strongest correlations between ∣Vz ∣ and major hurricanes occur (15, 16). Although there is substantial interannual variability in ∣Vz ∣, primarily associated with ENSO, this is being modulated by the obvious multidecadal-scale fluctuations. These fluctuations show a switch from conducive (high percentages of low ∣Vz ∣) to suppressed (low percentages of low ∣Vz ∣) conditions in 1970, almost coincident with the shift in major hurricanes (Fig. 1), NTC (35) and SSTs (Fig. 2B). In Fig. 3, however, the switch back to conducive conditions appears to start in 1988 (44), 7 years earlier than the switch for the other parameters. Even though 1991 through 1994 exhibit a short-term return to less conducive values, 1988 through 1990 had the most favorable values since 1969. Figure 2 shows some evidence of North Atlantic SST warming for a few years around 1988 followed by several cooler years in the early 1990s before the major warming in 1995. The warming around 1988 is much more evident in the Atlantic multidecadal mode values for ASO and in the actual ASO SSTs for the MDR (not shown). Nonetheless, the dominant shift to warmer values clearly takes place in 1995, which is when occurrences of more than three major hurricanes and hyperactive years [NTC ≥ 150%; (35)] resumed.

Figure 3

Percentage of south-central portion (10°–14°N, 20°– 70°W) of the main development region (see Fig. 2A) where ∣Vz ∣ < 6 m s−1 (values extremely conducive for tropical cyclone development) for ASO. Dashed curved line is 5-year running mean. Higher and lower percentages indicate conditions that are more or less conducive to development, respectively.

For almost every measure of tropical cyclone activity, the differences between the warm and cold phases of the mode are statistically significant (34, 44). The single exception is the number of U.S. Gulf Coast landfalling major hurricanes. This is because the Gulf of Mexico activity does not have a significant relationship with ∣Vz ∣ fluctuations in the MDR (11, 12, 15) or to the multidecadal North Atlantic SST fluctuations (Fig. 2A). The greatest differences (ratios) are for major hurricanes, hurricane days, U.S. East Coast major hurricane landfalls, and especially Caribbean hurricanes and U.S. damage. The Caribbean Sea has shown dramatic changes in hurricane activity—averaging 1.7 occurrences per year during the warm periods compared with only 0.5 per year during the cold period (34). The current warm period has produced an average of 2.5 occurrences per year with an unprecedented (since 1944) six hurricanes in the region during 1996. These multidecadal changes are illustrated in Fig. 4, which clearly shows the enhancement of overall Caribbean hurricane activity during warmer periods. Not only is the entire Caribbean region much less active during the colder period (Fig. 4A), but the only hurricanes that developed during that period in the Caribbean Sea east of ∼73°W formed during the two intermittent short warming periods (1979–1981 and 1987–1990) discussed earlier. Large multidecadal fluctuations of major hurricane landfalls are especially evident for the U.S. East Coast from the Florida peninsula to New England and are illustrated inFig. 5. No major hurricanes made landfall from 1966–1983. This relatively quiet period was similar to, but more extreme than, the low activity period during the first two decades of the 20th century. In contrast, during 1947–1965, 14 major hurricanes struck the East Coast (13). Overall, the United States has experienced about five times as much in median damages from tropical storms and hurricanes during the warm (high activity) than during the cold (low activity) phases of the Atlantic multidecadal mode (44).

Figure 4

Contrast of Caribbean hurricanes between colder (A) and warmer (B) values of the Atlantic multidecadal mode. The solid green (thin) and red (thick) lines indicate where the hurricanes were at nonmajor and major hurricanes intensities, respectively. Tropical storm intensity is indicated by dotted lines in cases where a hurricane weakened to tropical storm strength and then re-intensified to hurricane status. The years are similar to (34) except that the first nine warmer years (1944–1952) are not included to make the number of colder and warmer years equal. The colder years (24 years) include 1971–1994. The warmer years (24 years) include 1953–1970 and 1995–2000.

Figure 5

Contrast of U.S. East Coast major hurricane landfalls between colder (A) and warmer (B) values of the Atlantic multidecadal mode. The solid red lines indicate where the storms were at major hurricane intensity. The years are like those in (44) except that the first four warmer years (1899–1902) are not included to make the number of colder and warmer years similar. Colder years (47 years) include 1903–1925 and 1971–1994. Warmer years (51 years) include 1926–1970 and 1995–2000.

The Atlantic tropical cyclone record, which (except for U.S. landfall data) is not considered reliable before 1944 (33), shows less than one complete cycle of the multidecadal signal. The record for the SST signal represented by the Atlantic multidecadal mode (Fig. 2B), however, which has demonstrated a robust relation to the observed activity, shows about two complete cycles-—with some proxy records extending back several additional cycles (42). In addition, U.S. landfall data are able to show almost two periods of the signal (13, 44). Because of the multidecadal scale of the Atlantic SST variability portrayed here, the shift since 1995 to an environment generally conducive to hurricane formation—warmer North Atlantic SSTs and reduced vertical wind shear—is not likely to change back soon (45). This means that during the next 10 to 40 years or so, most of the Atlantic hurricane seasons are likely to have above average activity, with many hyperactive, some around average, and only a few below average. Furthermore, consistent with experience since the active phase began in 1995, there would be a continuation of significantly increased numbers of hurricanes (and major hurricanes) affecting the Caribbean Sea and basin-wide numbers of major hurricanes. The Gulf of Mexico, however, is expected to see only minor differences. Tragic impacts of the heightened activity have already been felt, especially in the Caribbean [e.g., Hurricanes Georges and Mitch (46)]. In addition, an increase in major hurricane landfalls affecting the U.S. East Coast is anticipated, but has not yet materialized (47).

One may ask whether the increase in activity since 1995 is due to anthropogenic global warming. The historical multidecadal-scale variability in Atlantic hurricane activity is much greater than what would be “expected” from a gradual temperature increase attributed to global warming (5). There have been various studies investigating the potential effect of long-term global warming on the number and strength of Atlantic-basin hurricanes. The results are inconclusive (48). Some studies document an increase in activity while others suggest a decrease (49). Tropical North Atlantic SST has exhibited a warming trend of ∼0.3°C over the last 100 years (38); whereas Atlantic hurricane activity has not exhibited trendlike variability, but rather distinct multidecadal cycles as documented here and elsewhere (12,13, 17). The extreme activity in 1995 has been attributed in part to the record-warm temperatures in the North Atlantic (25). The possibility exists that the unprecedented activity since 1995 is the result of a combination of the multidecadal-scale changes in Atlantic SSTs (and vertical shear) along with the additional increase in SSTs resulting from the long-term warming trend. It is, however, equally possible that the current active period (1995–2000) only appears more active than the previous active period (1926–1970) due to the better observational network now in place. During the previous active period, only 1966–1970 had continual satellite coverage (33, 50). Further study is essential to separate any actual increase from an apparent one due to more complete observations.

Although increased activity during a particular year does not automatically mean increased storm-related damages (51), years with high activity have a greater overall potential for disaster than years with low activity. Increased occurrence combined with dramatic coastal population increases during the recent lull, add up to a potential for massive economic loss (13). In addition, there remains a potential for catastrophic loss of life in an incomplete evacuation ahead of a rapidly intensifying system. Government officials, emergency managers, and residents of the Atlantic hurricane basin should be aware of the apparent shift in climate and evaluate preparedness and mitigation efforts in order to respond appropriately in a regime where the hurricane threat is much greater than it was in the 1970s through early 1990s.

  • * To whom correspondence should be addressed. E-mail: Stanley.Goldenberg{at}noaa.gov

REFERENCES AND NOTES

View Abstract

Cited By...

Subjects

Navigate This Article