ライフサイエンスコーパス: ENSO

1 ENSO amplitude forecast errors are most strongly associa

2 ENSO effects are location-specific and in southeastern U

3 ENSO exposure was based on the Multivariate ENSO Index.

4 ENSO impacts are much wider than previously thought.

5 ENSO was associated more with vector-borne disease [rela

6 under varying climate scenarios. The 2015/17 ENSO event was coupled with a positive PDO and resulted

7 lant water potentials in HSF during the 2015-ENSO, greater xylem embolism resistance maintained simil

8 ariability and highlight the need to address ENSO reconstruction with a geographically diverse networ

9 have been limited to short lead times after ENSO sea surface temperature (SST) anomaly has already d

10 heat exposure in most ecoregions and in all ENSO phases.

11 This is based on analysis of all ENSO events in the past 136 years using multiple long-te

12 Yields varied among ENSO phases from 1971-2013, with greater yields observed

13 strong zonal gradient to one with amplified ENSO and weak gradient.

14 soon (WAM) as critical factors in amplifying ENSO's response to insolation forcing through changes in

15 e relationship between dolphin abundance and ENSO, Southern Annular Mode, austral season, rainfall, s

16 ategies quantifying both, climate change and ENSO effects on month-specific growing season climate co

17 d between tropical wetland CH4 emissions and ENSO events, which was caused by the combined time lag e

18 s due to frequency increases of both WWV and ENSO.

19 among which statistical models approximating ENSO evolution by linear dynamics have received signific

20 Because ENSO has some predictive skill with lead times of severa

21 Here we investigate the connections between ENSO, local environmental conditions, and childhood diar

22 The tight coupling between ENSO and the annual cycle is particularly pronounced ove

23 , which is the main atmospheric link between ENSO and the East Asian Monsoon system, can be explained

24 d previous research has shown a link between ENSO patterns and cholera in Bangladesh.

25 ted equally to the difference in NEP between ENSO year 1998 and non-ENSO year 2000.

26 We find a robust relationship between ENSO and southeast Asian SATs wherein virtually all Apri

27 cks, suggesting a tight relationship between ENSO strength and background climate conditions.

28 se network of sites to characterise how both ENSO, and its impacts, vary in a changing climate.

29 region of northwest Australia is muted, but ENSO-driven changes to the monsoon may have complemented

30 phin abundance was significantly affected by ENSO, and that the magnitude of the effect was dependent

31 .9 K(2) on 1-5 year timescales, dominated by ENSO processes.

32 non-super typhoons are little influenced by ENSO, and the changes are mostly by the addition of supe

33 Since a unified and complete ENSO theory has yet to be established, people often use

34 By contrast, ENSO was associated with more enteric disease in non-Wes

35 ng feedbacks as the major factor controlling ENSO strength on millennial time scales.

36 deficiencies in capturing the developing CP-ENSO and anomalous Asian Low.

37 cal Pacific El Nino Southern Oscillation (CP-ENSO) and its atmospheric teleconnections back to the No

38 ral-Pacific El Nino-Southern Oscillation (CP-ENSO), the rapid deepening of the Asian Low and the stre

39 ation function between the KE and the PMM/CP-ENSO indices exhibits a significant sinusoidal shape cor

40 This dynamics pathway (KE->PMM/CP-ENSO->KE) may provide a new mechanistic basis to explain

41 und 1500-1650 CE, from a state with dampened ENSO and strong zonal gradient to one with amplified ENS

42 During the early deglaciation, ENSO characteristics change drastically in response to m

43 to which background climate state determines ENSO behavior remains in question.

44 he Walker circulation anomalies at different ENSO phases all resemble those in nature.

45 bution of TC genesis locations for different ENSO conditions does not completely explain these result

46 f increased or decreased flood hazard during ENSO events is much more complex than is often perceived

47 lower net ecosystem production (NEP) during ENSO year 1998 compared with non-ENSO year 2000 in a Cos

48 ar and chaotic dynamics (particularly during ENSO initiation), such models have limited skill for lon

49 ons than the changes in precipitation during ENSO periods.

50 ises the modal temperature threshold of each ENSO cycle.

51 ked to a multicentury perturbation of either ENSO-like variability or the ITCZ, imply a high sensitiv

52 likelihood of adverse impacts during extreme ENSO events.

53 e sub-prediction results to obtain the final ENSO prediction results.

54 hat is, the NTA SST triggering the following ENSO via a subtropical teleconnection mechanism) process

55 SO teleconnections is not only important for ENSO, but acts as a primary mechanism to filter (e.g. re

56 A new physics-based empirical model for ENSO is constructed that significantly outperforms curre

57 Over the past decades, numerous models for ENSO prediction have been developed, among which statist

58 n ocean thermal structure are precursors for ENSO events and their initial specification is essential

59 However, forecasting ENSO is one of the most difficult problems in climate sc

60 a greater cumulative oceanic heat loss from ENSO thermal damping reduces stratification of the upper

61 statistically optimal predictions of future ENSO states as conditional expectations, given noisy and

62 y suppressed by internal variability, future ENSO variability is likely to be enhanced, and vice vers

63 DV generated internally in the tropics (e.g. ENSO residuals), is inherently unpredictable and not wel

64 s from the central tropical Pacific to gauge ENSO's response to large volcanic eruptions of the last

65 new western Pacific perspective on Holocene ENSO variability and highlight the need to address ENSO

66 onditions, are essential to anticipating how ENSO phases may respond under future climate scenarios.

67 However, ENSO predictability has been reduced in the 21(st) centu

68 f coupled internal variability on changes in ENSO under anthropogenic global warming using the Commun

69 lity (BJ) index analysis, enhanced errors in ENSO amplitude with forecast lead times are found to be

70 nd physical weathering rates, especially, in ENSO-influenced regions.

71 ific Ocean, leading to a smaller increase in ENSO variability under subsquent greenhouse warming.

72 f the greenhouse-warming-induced increase in ENSO variability(29) is initially suppressed by internal

73 e with the effects of natural modulations in ENSO sea surface temperature (SST) metrics, as well as h

74 to four years, and matched periodicities in ENSO conditions.

75 ge significantly over time or with shifts in ENSO.

76 variability in the Pacific including that in ENSO and the PSHs during recent decades.

77 rors in the thermocline feedback and thus in ENSO amplitude.

78 of ocean-atmosphere internal variability in ENSO projections.

79 M due to anthropogenic warming may influence ENSO variability in the future as well.

80 conditions induces vastly different initial ENSO variability, which systematically affects its respo

81 t Glacial Maximum (LGM) provide insight into ENSO behavior when global boundary conditions (ice sheet

82 The 'charging' (that is, ENSO imprinting the North Tropical Atlantic (NTA) sea su

83 This self-modulation linking ENSO variability across time presents a different perspe

84 parent mismatch in both timing and location: ENSO peaks in winter and its surface warming occurs most

85 hibited temporary reductions following major ENSO events, but no overall decline.

86 forcings may have dwarfed the fairly modest ENSO response to precessional insolation changes simulat

87 growth rates (r = -.94) and the Multivariate ENSO Index (MEI) for all years (r = .74).

88 nfall, solar radiation, and the Multivariate ENSO Index, respectively.

89 ENSO exposure was based on the Multivariate ENSO Index.

90 e of the forced response relative to natural ENSO variability.

91 chrony between the positive PDO and negative ENSO (i.e., La Nina) was associated with peaks in annual

92 consistencies exist between El Nino/La Nina (ENSO) cycles and precipitation in the historical record;

93 winter of 2015, there was a strong El Nino (ENSO) event, resulting in significant anomalies for mete

94 erence in NEP between ENSO year 1998 and non-ENSO year 2000.

95 There is also clear evidence that other non-ENSO climatic variations have a strong control on spatia

96 NEP) during ENSO year 1998 compared with non-ENSO year 2000 in a Costa Rican tropical rainforest.

97 which enables the model to capture observed ENSO statistics such as the probability density function

98 While climate models reproduce observed ENSO amplitude relatively well, the majority still simul

99 l conditions varied markedly due to observed ENSO states: El Nino (2015) and neutral (2016-2017).

100 a significant extratropical forcing agent of ENSO.

101 The frequency change of ENSO and WWV were linked to a westward shift of the Bjer

102 The second most predictable component of ENSO evolution, with lower prediction skill and smaller

103 ctive for the most predictable components of ENSO.

104 however, the direct ocean thermal control of ENSO on TCs has not been taken into consideration becaus

105 ections, resulting from opposing controls of ENSO on precipitation between the Northern Hemisphere (p

106 ically captures the statistical diversity of ENSO.

107 Therefore, better simulating the dynamics of ENSO asymmetry potentially reduces uncertainty in future

108 erspective for understanding the dynamics of ENSO variability on multiple timescales in a changing cl

109 supports that the non-stationary effects of ENSO can be propagated from tropical areas to semi-arid

110 s caused by the combined time lag effects of ENSO events on precipitation and temperature over tropic

111 nd linear model selection showed evidence of ENSO-driven synchrony in growth among all four taxa at i

112 El Nino and La Nina events, the extremes of ENSO climate variability, influence river flow and flood

113 ur study suggests that reliable forecasts of ENSO strongly rely on correctly modeling the meridional

114 o investigate the amplitude and frequency of ENSO and interdecadal climate events.

115 ure changes in the strength and frequency of ENSO events are likely to have major consequences for bo

116 trends, were used to evaluate the impact of ENSO on disease incidence over lags of up to 12 mo.

117 We studied the impact of ENSO on infectious diseases in four census regions in th

118 The impact of ENSO suggests that warmer temperatures and extreme varia

119 elds in many regions, the overall impacts of ENSO on global yields are uncertain.

120 from 2000 to 2014 to explore the impacts of ENSO on variability of semi-arid ecosystems, using the E

121 However, the impacts of ENSO precursors on Tropical Pacific Decadal-scale Variab

122 trate a new picture of the global impacts of ENSO throughout its whole lifecycle based on the rich la

123 ea coupling region will cause an increase of ENSO frequency, as the corresponding zonal advection fee

124 on analyses show that large-scale indices of ENSO variability can predict 20% to 45% of annual runoff

125 The influence of ENSO on monsoon precipitation in this region of northwes

126 r study indicates that an intensification of ENSO will have negative effects on some mangrove forests

127 n increase in the frequency and intensity of ENSO events predicted in the coming decades threatens a

128 significantly contribute to the intensity of ENSO in October-December by weakening the Walker circula

129 ionships with the Nino-4 index (a measure of ENSO status), with positive growth patterns occurring du

130 The periodic nature of ENSO may make it a useful natural experiment for evaluat

131 ending on time of year and the occurrence of ENSO events, settlement of Hawai'i and New Zealand is po

132 Outlooks of ENSO and its impacts often follow a two-tier approach: p

133 omponent (MSN EOF1) is the decaying phase of ENSO during the Northern Hemisphere spring, followed by

134 This result suggests that decay phase of ENSO is more predictable than the growth phase.

135 on surface water storage, the warm phase of ENSO preconditions the lower Mississippi River to be vul

136 en associated with the 1998 La Nina phase of ENSO.

137 e conditions, suggesting that both phases of ENSO provide a favorable background for the occurrence o

138 However, the current picture of ENSO global impacts widely used by forecasting centers a

139 h performs well in the advance prediction of ENSO and will be of great guiding significance in studyi

140 ate anomalies, and the advance prediction of ENSO is always an important and challenging scientific i

141 Here, we present a reconstruction of ENSO in the eastern tropical Pacific spanning the past 1

142 To understand the significance of ENSO and other climatic oscillations to heat stress in t

143 problem about the target period slippage of ENSO.

144 According to the classical theories of ENSO, subsurface anomalies in ocean thermal structure ar

145 (SOI), to predict the development trends of ENSO through appropriate numerical simulation models.

146 se findings demonstrate the potential use of ENSO as a long-lead prediction tool for childhood diarrh

147 s used to indicate the internal variation of ENSO.

148 global warming requires quantitative data on ENSO under different climate regimes.

149 Long-term perspectives on ENSO behaviour, under changing background conditions, ar

150 little is known about the feedback of TCs on ENSO.

151 the signal of El Nino-Southern Oscillation (ENSO) activity became erratic.

152 e temperature, El Nino-Southern Oscillation (ENSO) activity, and the tropical Pacific zonal gradient

153 onship between El Nino-Southern Oscillation (ENSO) and ENP TCs.

154 iations in the El Nino-Southern Oscillation (ENSO) and GMSL.

155 The El Nino Southern Oscillation (ENSO) and other climate patterns can have profound impac

156 rmine that the El Nino-Southern Oscillation (ENSO) and the Southern Annular Mode (SAM) are strongly a

157 The El Nino-Southern Oscillation (ENSO) and the variability in the Pacific subtropical hig

158 prevalence and El Nino Southern Oscillation (ENSO) cycles was examined using cross-wavelet analyses a

159 del (LSM), and El Nino-Southern Oscillation (ENSO) data in an autoregressive model with exogenous var

160 olution of the El Nino-Southern Oscillation (ENSO) during the Holocene remains uncertain.

161 trength during El Nino Southern Oscillation (ENSO) events can indicate future behavior under climate

162 nce the 1980s, El Nino Southern Oscillation (ENSO) events have been more frequently associated with c

163 remote effect, El Nino Southern Oscillation (ENSO) events in the equatorial Pacific Ocean alter preci

164 El Nino Southern Oscillation (ENSO) events modulate oceanographic processes that contr

165 y occur during El Nino-Southern Oscillation (ENSO) events originating in the Eastern Tropical Pacific

166 e influence of El Nino Southern Oscillation (ENSO) events, and "shortest-hop" trajectories, demonstra

167 t occur during El Nino Southern Oscillation (ENSO) events.

168 ponents of the El Nino-Southern Oscillation (ENSO) evolution in real-time multi-model predictions are

169 application of El Nino-Southern Oscillation (ENSO) forecasts, including the development of successful

170 status of the El Nino-Southern Oscillation (ENSO) had the highest correlation with adult growth chro

171 El Nino Southern Oscillation (ENSO) has a strong influence on the U.S. climate and is

172 orecasting the El Nino-Southern Oscillation (ENSO) has been a subject of vigorous research due to the

173 El Nino-Southern Oscillation (ENSO) has been shown to affect diarrhea dynamics in Sout

174 ication of the El Nino Southern Oscillation (ENSO) has increased variation in sea level.

175 ility like the El Nino-Southern Oscillation (ENSO) has proven challenging, due in part to the limited

176 The El Nino Southern Oscillation (ENSO) has significant impact on global climate and seaso

177 phases of the El Nino-Southern Oscillation (ENSO) have major impacts on regional rainfall patterns a

178 modes such as El Nino Southern Oscillation (ENSO) influence population dynamics in many species, inc

179 we show that El Nino - Southern Oscillation (ENSO) is a main driver of the interannual variability in

180 El Nino-Southern Oscillation (ENSO) is a major source of global interannual variabilit

181 The El Nino Southern Oscillation (ENSO) is highly dependent on coupled atmosphere-ocean in

182 The El Nino-Southern Oscillation (ENSO) is the dominant interannual variability of Earth's

183 The El Nino-Southern Oscillation (ENSO) is the dominant interannual variability of Earth's

184 El Nino-Southern Oscillation (ENSO) is the dominant interseasonal-interannual variabil

185 The El Nino-Southern Oscillation (ENSO) is the main driver of interannual climate extremes

186 anding how the El Nino-Southern Oscillation (ENSO) may change with climate is a major challenge, give

187 esponse to the El Nino-Southern Oscillation (ENSO) of 2015.

188 Although the El Nino/Southern Oscillation (ENSO) often affects seasonal temperature and precipitati

189 impact of the El Nino-Southern Oscillation (ENSO) on CH4 emissions from wetlands remains poorly quan

190 luences of the El Nino Southern Oscillation (ENSO) on global groundwater storage.

191 ary effects of El Nino Southern Oscillation (ENSO) on regional forest carbon capture.

192 ced changes in El Nino-Southern Oscillation (ENSO) or sea-surface temperature do not seem to have a s

193 El Nino-Southern Oscillation (ENSO) phases (La Nina, neutral, and El Nino years) appea

194 impact of the El Nino/Southern Oscillation (ENSO) phenomenon and long-term warming on regional SAT e

195 te change, the El Nino Southern Oscillation (ENSO) phenomenon would be an important factor influencin

196 The El Nino-Southern Oscillation (ENSO) phenomenon, the most pronounced feature of interna

197 The El Nino-Southern Oscillation (ENSO) results from the instability of and also modulates

198 The El Nino-Southern Oscillation (ENSO) shapes global climate patterns yet its sensitivity

199 The El Nino-Southern oscillation (ENSO) simulated in the Community Earth System Model of t

200 esponse of the El Nino-Southern Oscillation (ENSO) to global warming requires quantitative data on EN

201 al Pacific and El Nino-Southern Oscillation (ENSO) variability after 2000 are documented.

202 onal winds and El Nino-Southern Oscillation (ENSO), and negatively affected by sea ice concentration

203 rred to as the El Nino-Southern Oscillation (ENSO), are not only highly consequential(1-6) but also s

204 ssociated with El Nino Southern Oscillation (ENSO), but we highlight the relevance of the long-term i

205 changes in the El Nino Southern Oscillation (ENSO), especially at latitudes lower than 34 degrees S.

206 ursors" of the El Nino Southern Oscillation (ENSO), have been shown to independently trigger the ENSO

207 s, such as the El Nino Southern Oscillation (ENSO), might have on weathering fluxes.

208 ions including El Nino Southern Oscillation (ENSO), North Atlantic Oscillation (NAO), and Pacific Dec

209 ice cover, the El Nio Southern Oscillation (ENSO), the Atlantic Nio and the Indian Dipole Mode.

210 ion (MDR), the El Nino-Southern Oscillation (ENSO), the North Atlantic Multidecadal Oscillation (AMO)

211 nt mode of the El Nino/Southern Oscillation (ENSO), the primary driver of modern TC variability.

212 El Nino-Southern Oscillation (ENSO), which is one of the main drivers of Earth's inter

213 The El Nino-Southern Oscillation (ENSO), which originates in the Pacific, is the strongest

214 ion to El Nino and the Southern Oscillation (ENSO)--in particular, extreme El Nino and La Nina events

215 e amplitude of El Nino Southern Oscillation (ENSO)-driven sea surface temperature variability.

216 g-term data on El Nino Southern Oscillation (ENSO)-driven synchrony of climate impacts on both terres

217 the 1997/1998 El Nino Southern Oscillation (ENSO)-the strongest on record-combined with an unprecede

218 Mode (SAM) and El Nino Southern Oscillation (ENSO).

219 dulated by the El Nino-Southern Oscillation (ENSO).

220 iated with the El Nino/Southern Oscillation (ENSO).

221 largely by the El Nino-Southern Oscillation (ENSO).

222 changes in the El Nino/Southern Oscillation (ENSO).

223 ynamics of the El Nino Southern Oscillation (ENSO).

224 ability of the El Nino-Southern Oscillation (ENSO).

225 s, such as the El Nino-Southern Oscillation (ENSO).

226 b" and extreme El Nino Southern Oscillation (ENSO).

227 esponse to El Nino and Southern Oscillation (ENSO).

228 The "El Nino Southern Oscillation" (ENSO) occurs irregularly and is associated with changing

229 atural modulations; however, central Pacific ENSO amplitude significantly decreases, to an extent com

230 Changes in eastern Pacific ENSO SST metrics due to climate change are secondary to

231 In particular, ENSO influences the yearly variations of tropical cyclon

232 chrony between the positive PDO and positive ENSO (i.e., El Nino) was associated with peaks in chloro

233 often follow a two-tier approach: predicting ENSO sea surface temperature anomaly in tropical Pacific

234 of this feedback is essential for predicting ENSO's behavior under future climate conditions.

235 tly outperforms current models in predicting ENSO intensity from July to December and addressing the

236 tional nonlinearities reproduces a realistic ENSO cycle with intermittent El Nino and La Nina events

237 ironmental conditions associated with recent ENSO cycles may have influenced the patterns in disease

238 relative to preindustrial climate can reduce ENSO variability by 25%, more than twice the decrease ob

239 equatorial cold tongue, resulting in reduced ENSO variability during the LGM compared to the Late Hol

240 o are invaluable archives to detect regional ENSO and PDO impacts, and their interaction with the Asi

241 opical wetlands respond strongly to repeated ENSO events, with negative anomalies occurring during El

242 tatistical relationship between seasonality, ENSO, and river discharge, with significantly higher val

243 primacy of the upwelling feedback in shaping ENSO behavior across many different background states su

244 historical record; for example, significant ENSO-precipitation correlations were present in only 31%

245 climate models, we here show that simulated ENSO asymmetry is largely proportional to subsurface non

246 tial specification is essential for skillful ENSO forecast.

247 s that intensity of disease activity in some ENSO-teleconnected regions were approximately 2.5-28% hi

248 Climate cycle indices of spring ENSO, summer NAO, and winter or spring PDO accounted for

249 s suggest that those models showing a strong ENSO response to volcanic forcing may overestimate the s

250 Here, we demonstrate that ENSO drives intrabasin variability of ENP TCs, with enha

251 We found that ENSO variance was close to the modern level in the early

252 These findings highlight that ENSO-induced changes in salinity, plankton biomass, and

253 We show that ENSO and PDO together predicted (i) maximum sea-surface

254 We show that ENSO exerts strong and widespread influences on both flo

255 ost of new paleoclimate records suggest that ENSO internal variability or other external forcings may

256 Modeling studies suggest that ENSO is sensitive to sulfate aerosol forcing associated

257 These results suggest that ENSO was not tied directly to the east-west temperature

258 The ENSO amplitude simulated in the feedback run is more acc

259 The ENSO can explain 49% of interannual variations for tropi

260 tionship between wind burst activity and the ENSO.

261 However, because the ENSO phenomenon is a highly complex and dynamic model an

262 y the magnitude of changes that followed the ENSO-induced SST warming that affected the Indian Ocean

263 The ocean forcing from the ENSO is secondary and tends to be confined in the tropic

264 torial Pacific played a decisive role in the ENSO response to LGM climate.

265 a novel approach to noticeably increase the ENSO prediction skill beyond the spring predictability b

266 sified during the past 2 decades, making the ENSO more complicated and harder to predict.

267 d Indo-Pacific climate, the character of the ENSO cycle, and the hiatus in global surface warming.

268 Due to the weaker amplitude of the ENSO forcing, these sub-seasonal atmospheric responses c

269 emissions to investigate the impacts of the ENSO on CH4 emissions in tropical wetlands for the perio

270 e the spatial extent and distribution of the ENSO-induced plankton biomass variability.

271 t activity has a direct causal effect on the ENSO variability: in particular, it intermittently trigg

272 surface salinities, which are linked to the ENSO system, influenced the annual growth of fishes, tre

273 have been shown to independently trigger the ENSO feedbacks in the tropics and its teleconnections to

274 LIM), while significantly improving upon the ENSO predictability "spring barrier".

275 This ENSO-thermocline relationship implicates upwelling feedb

276 t on the dynamics linking ENP TC activity to ENSO, and highlight the importance of improving CAGW rep

277 orthern Hemisphere (positively correlated to ENSO) and the Southern Hemisphere (negatively correlated

278 outhern Hemisphere (negatively correlated to ENSO).

279 cy has strong interannual variability due to ENSO (El-Nino/Southern Oscillation), with more events un

280 faster responses of semi-arid ecosystems to ENSO than the Northern Hemisphere.

281 provide significant cross-scale feedback to ENSO.

282 uence from extra-tropical ENSO precursors to ENSO (tropics) to extra-tropical ENSO teleconnections is

283 cific warming pattern is linearly related to ENSO amplitude change in response to greenhouse warming.

284 nly driven by convective activity related to ENSO and that the barotropic nature of the subtropical i

285 emi-arid ecosystem productivity responded to ENSO in opposite ways between two hemispheres, which may

286 super typhoons to TC activity in response to ENSO, where the Southern Oscillation Index (SOI) is used

287 problem'(12,16,17) and too-weak responses to ENSO(15).

288 hat the responses of semi-arid vegetation to ENSO occur in opposite directions, resulting from opposi

289 hat the dynamic sequence from extra-tropical ENSO precursors to ENSO (tropics) to extra-tropical ENSO

290 ecursors to ENSO (tropics) to extra-tropical ENSO teleconnections is not only important for ENSO, but

291 In WA, ENSO affects the strength of the Leeuwin Current (LC), t

292 r than the canonical eastern Pacific warming ENSO (EPW).

293 on the extreme phases rather than the whole ENSO lifecycle.

294 but instead include elements associated with ENSO SST precursors and SST anomalies in the central/wes

295 SST anomaly patterns usually associated with ENSO, but instead include elements associated with ENSO

296 ocation, and not necessarily associated with ENSO, can significantly influence USWC conditions and en

297 processes, which are highly correlated with ENSO variations, contribute about equally to observed in

298 en cholera and climate patterns coupled with ENSO forecasting could be used to notify countries in Af

299 For the past 30 years, ENSO forecasts have been limited to short lead times aft

300 ell as its delicate feedback with the zonal (ENSO) mode.