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Tropical Easterly Jet

The Tropical Easterly Jet (TEJ) is a prominent upper-tropospheric easterly wind maximum in the tropics, active during the Northern Hemisphere summer from late June to early September, spanning longitudinally from the east coast of Vietnam across the Indian Ocean to West Africa at latitudes of approximately 10°–20°N and altitudes corresponding to 100–200 hPa pressure levels.^[1]^[2] It features core wind speeds often exceeding 40 m/s, driven by the reversal of the meridional temperature gradient resulting from intense diabatic heating over continental landmasses like the Tibetan Plateau contrasted against the cooler surrounding oceans.^[3]^[1] As a key dynamical component of the Asian and West African summer monsoon systems, the TEJ facilitates upper-level easterly momentum transport and divergence that enhances convective activity and rainfall north of its inflow region, with stronger intensities linked to robust monsoon precipitation over India and the Sahel.^[1] Its core position exhibits variability, including northward shifts to around 20°N during monsoon breaks over India, which correlate with suppressed rainfall, and interannual fluctuations influenced by sea surface temperature anomalies in the Pacific and Indian Oceans.^[2]^[1] The jet's formation and maintenance underscore the primacy of land-sea thermal contrasts in tropical circulation, distinguishing it from westerly subtropical jets and highlighting its role in bridging tropical and subtropical monsoon dynamics without reliance on frontal boundaries.^[3]

Physical Characteristics and Meteorology

Core Features and Seasonal Cycle

The Tropical Easterly Jet (TEJ) manifests as a narrow band of strong easterly winds in the upper troposphere, with its core typically situated between 100 and 150 hPa pressure levels, corresponding to altitudes of approximately 14-16 km.^[2]^[4] This jet is centered around 10°-15°N latitude over the tropical Indian Ocean, extending longitudinally from the Arabian Sea westward toward Africa, and features maximum zonal wind speeds of 30-40 m/s, often exceeding 35 m/s during peak conditions.^[4]^[5]^[2] The flow exhibits a pronounced vertical shear, with easterlies intensifying from about 200 hPa upward to the jet core, driven by thermal contrasts that reverse the typical subtropical westerly regime in the tropics.^[4] Spatially, the TEJ spans a latitudinal width of roughly 10°-20°, with its meridional structure showing deceleration poleward of the core due to Coriolis effects and equatorward weakening toward the intertropical convergence zone.^[6] Zonal extent covers key monsoon domains, including the Indian subcontinent and Sahel regions, where it overlies mid-level westerlies like the African Easterly Jet, creating a characteristic shear profile that modulates convective outflows.^[1] Observational data from reanalyses indicate core wind speeds crossing 30 m/s consistently in monsoon months at these levels, with sub-daily fluctuations tied to diurnal heating cycles.^[6] The seasonal cycle of the TEJ aligns closely with the boreal summer monsoon, initiating in late June as upper-level easterlies strengthen over the heated Asian landmass, reaching onset thresholds of sustained speeds above 20 m/s by early July.^[2] Peak intensity occurs in July-August, when maximum winds and spatial coherence are highest, coinciding with maximum solar insolation and land-sea thermal gradients.^[4]^[6] Decay begins in September, with winds weakening below 20 m/s by October as cooling reduces the meridional temperature gradient, leading to full dissipation by November and reversion to westerly flows in winter.^[5] This cycle exhibits interannual variability, with stronger jets linked to enhanced monsoon convection, though long-term trends show modest weakening in core speeds over recent decades.^[6]

Vertical and Horizontal Structure

The Tropical Easterly Jet (TEJ) displays an expansive horizontal structure during boreal summer, extending longitudinally from Indonesia eastward across the northern Indian Ocean to the Atlantic Ocean, with intensified easterly flows over southern Asia, the Arabian Peninsula, and eastern Africa.^[4]^[7] A secondary branch originates near 10°N along Africa's west coast, dissipating over the eastern Atlantic, while the primary core aligns around 15°N latitude overlying landmasses rather than oceanic regions like the Pacific.^[7] Spatial variability in the jet's core manifests in three primary modes—eastern, northwestern, and southwestern—driven by differences in zonal circulation and meridional temperature gradients.^[8] In the vertical dimension, the TEJ occupies the upper troposphere to lower stratosphere, spanning pressure levels from 300 hPa to 70 hPa, with its axis of maximum easterly winds centered near 150 hPa (approximately 14 km altitude).^[9]^[4] The strongest winds form within a relatively thin layer of about 3 km (10,000 feet) thickness above 250 hPa, peaking at speeds exceeding 35 m/s during July–August monsoon maxima and occasionally reaching 50 m/s (110 mph).^[4]^[7] This profile generates pronounced easterly vertical shear, averaging -45 m/s from 150 hPa to 850 hPa, which enhances tropospheric stability and modulates convection beneath the jet.^[4]

Formation Dynamics

Thermal and Circulatory Drivers

The Tropical Easterly Jet (TEJ) forms primarily through thermal wind balance driven by upper-tropospheric meridional temperature gradients established during boreal summer. Sensible heating from the elevated Tibetan Plateau, reaching surface temperatures exceeding 30°C in July and elevating the plateau's thermal low to upper levels, combines with latent heat release from deep moist convection over the Indian Ocean and South Asia, where diabatic heating rates can surpass 2 K/day. This produces a temperature maximum centered around 20°-30°N, with gradients of approximately 1-2 K per degree latitude toward the subtropics, inverting the typical wintertime profile and yielding easterly vertical shear via the thermal wind equation: \frac{\partial u}{\partial p} \propto -\frac{R}{f p} \frac{\partial T}{\partial y}, where positive \frac{\partial T}{\partial y} (equatorward warming) generates upper-level easterlies peaking at 30-40 m/s near 150 hPa.^[5]^[8]^[10] Circulatory drivers integrate the TEJ into the hemispheric-scale monsoon response, where plateau-induced upper-level divergence from the Tibetan anticyclone—characterized by 200 hPa geopotential heights 100-200 m above zonal means—facilitates easterly outflow as the upper branch of the longitudinally oriented Walker-like circulation over Asia. This compensates low-level convergence from cross-equatorial flows, such as the Somali Jet exceeding 10 m/s, enforcing mass continuity and conserving absolute vorticity in the low-Coriolis tropics, thereby amplifying the jet through equatorial beta-plane dynamics. Observational reanalyses confirm the jet's core aligns with the anticyclone's divergent ridge, linking convective ascent rates of 5-10 cm/s over monsoon cores to sustained easterly momentum transport.^[11]^[12]^[13]

Role of Orographic Heating

Orographic heating over the Tibetan Plateau, primarily through sensible heat fluxes from its elevated surface (averaging 4,500 meters above sea level), contributes to the Tropical Easterly Jet (TEJ) by generating a tropospheric warm anomaly that drives upper-level divergence and anticyclonic circulation. Intense solar radiation on the plateau's barren, high-altitude terrain results in strong upward sensible heat transfer, warming the mid- to upper troposphere and inducing ascent over the region. This thermal forcing establishes a subtropical high-pressure system aloft, with the TEJ forming as the equatorward return flow of easterlies, accelerated by the conservation of absolute vorticity and Earth's rotation as air parcels descend southward toward the monsoon trough.^[14]^[15] Early theoretical frameworks, such as those developed by H. Flohn in the 1960s, emphasized this sensible heating as the primary driver of the TEJ, positing that the orography elevates the heat source, enabling efficient penetration of warmth into the upper troposphere and sustaining the jet's easterly winds at 100-150 hPa during boreal summer (June-August). The mechanism involves the plateau acting as a "heat pump," where surface heating reverses the meridional temperature gradient in the upper troposphere, favoring easterly shear and jet formation south of 20°N. Observational data from the 1950s-1970s, including pilot balloon and radiosonde measurements, supported this view by linking plateau surface temperatures exceeding 20°C in summer to TEJ core speeds of 30-40 m/s.^[16]^[14] However, general circulation model (GCM) sensitivity experiments reveal that orographic sensible heating plays a secondary role compared to latent heating from convection. Simulations removing Tibetan orography while retaining latent heat release reproduce the TEJ's location and strength with minimal deviation, whereas suppressing convective heating (e.g., by zeroing precipitation-related diabatic heating) shifts the jet poleward and weakens it significantly, indicating that monsoon-scale latent heat dominates the dynamical forcing. Orography amplifies sensible heating by about 20-30 W/m² relative to sea-level equivalents but contributes less than 10% to the overall upper-level momentum balance in these models.^[17]^[18]^[19] The southeastern Tibetan Plateau's orographic heating exerts a targeted influence on the TEJ's inflow region via two pathways: direct induction of easterly anomalies through local thermal wind response and remote propagation of Rossby waves that modulate double-jet structures upstream. Positive heating anomalies here (e.g., 2-5 K warmer than average in July) correlate with intensified TEJ cores, as quantified in reanalysis data from 1979-2020, though interannual variability is modulated more by convective feedbacks than pure sensible fluxes. Thus, while orographic heating preconditions the atmosphere in May-June—triggering initial monsoon onset and jet spin-up—its role transitions to supportive during peak season, sustaining the jet amid dominant latent processes.^[12]^[11]

Historical Discovery and Research

Early Observations (1950s-1970s)

The Tropical Easterly Jet (TEJ) was initially inferred from upper tropospheric wind analyses over India by P. R. Krishna Rao in 1952, who identified probable regions of easterly jet streams based on early radiosonde observations indicating strong easterly flows at 200 mb during the summer monsoon season.^[20] These findings drew from limited network data across southern Asia, highlighting accelerated easterlies near 15°N linked to seasonal heating contrasts.^[7] P. Koteswaram provided the first comprehensive documentation in 1958, describing the TEJ as a distinct upper-level easterly current overlying southern Asia with a core at approximately 100–150 mb, maximum speeds of 40–50 m s⁻¹ near 15°N, and extension westward toward Africa during boreal summer. ^[20] His analysis, utilizing radiosonde data from Indian stations and surrounding regions, demonstrated the jet's thermal wind balance driven by meridional temperature gradients, with cooler air over the heated Tibetan Plateau relative to warmer equatorial regions, and noted its onset coinciding with monsoon advancement, as evidenced by a specific case on July 25, 1955.^[21] Koteswaram emphasized the jet's role in upper tropospheric divergence supporting monsoon convection, distinguishing it from weaker easterlies elsewhere.^[11] In the 1960s, H. Flohn extended these observations through detailed investigations, linking the TEJ to the Tibetan anticyclone and elevated heating over the Himalayan-Tibetan region, which intensified the jet's easterly shear via baroclinic forcing.^[16] Flohn's 1964 work integrated Asian and African upper-air data, revealing the jet's longitudinal extent from Southeast Asia to West Africa at 200 mb, with core intensities varying inversely with subtropical westerlies, and suggested its modulation of cross-equatorial circulation.^[13] Observations during this era relied on expanding but still sparse global radiosonde networks, confirming seasonal activation from June to September and deactivation in winter, though vertical resolution limitations constrained precise shear profiling.^[1] By the 1970s, accumulated monsoon field campaigns, including enhanced Indian upper-air soundings, refined TEJ characteristics, quantifying typical core heights at 12–15 km and speeds of 30–40 m s⁻¹, while highlighting interannual variability tied to monsoon strength.^[14] These studies, building on Koteswaram and Flohn, used composite analyses to affirm the jet's causal role in sustaining upper-level anticyclonic outflow over monsoon heat sources, though data gaps over oceans persisted until satellite era inputs.^[22] Early research underscored the TEJ's empirical basis in direct wind measurements rather than theoretical constructs alone, establishing it as a key monsoon diagnostic.^[23]

Advancements in Understanding (1980s-Present)

In the 1980s, research on the Tropical Easterly Jet (TEJ) advanced through analyses linking its intensity to regional precipitation patterns, particularly over Sudan, where stronger jets were associated with reduced rainfall due to enhanced subsidence.^[24] These studies built on earlier observations by incorporating data from global field experiments like MONEX, enabling finer resolution of the jet's meridional extent and its role in modulating Sahelian aridity via dynamical feedbacks.^[25] Numerical modeling efforts during this period began simulating the TEJ's response to orographic heating, confirming its thermal wind structure through general circulation models (GCMs) that reproduced core speeds exceeding 30 m/s at 100-150 hPa over the Indian Ocean.^[7] The 1990s and early 2000s saw integration of satellite-derived winds and initial reanalysis datasets, such as ERA-40, which facilitated quantification of the TEJ's seasonal core at approximately 15°N and 100 hPa, with peak intensities in July-August.^[6] Interannual variability emerged as a focus, with studies identifying correlations between TEJ strength and ENSO phases, where El Niño events weakened the jet by altering upper-tropospheric divergence.^[6] By the mid-2000s, high-resolution observations from 1996-2008 revealed day-to-day fluctuations tied to convective outbreaks, underscoring the jet's sensitivity to intraseasonal oscillations like the Madden-Julian Oscillation.^[6] From the 2010s onward, multi-reanalysis comparisons highlighted consistent TEJ depictions across datasets like ERA-Interim and MERRA-2, validating its horizontal span from the western Pacific to Africa at speeds of 20-40 m/s, while noting biases in earlier products underestimating vertical shear. Evidence of a long-term weakening trend, approximately 10-15% since the mid-20th century, was documented using 60-year records, attributed primarily to anthropogenic greenhouse gas forcing reducing meridional temperature gradients.^[11] Climate model projections from CMIP6 ensembles predict further intensification of this decline by 11% in core speed under RCP8.5 scenarios, implying diminished monsoon outflow dynamics.^[26] Contemporary investigations have elucidated external forcings, such as the stratospheric quasi-biennial oscillation (QBO), where easterly QBO phases strengthen the TEJ by 2-5 m/s via altered wave propagation.^[27] Cluster analyses of jet core positions identify three modes—eastern, northwestern, and southwestern—linked to Indian Ocean dipole variations, with the northwestern shift enhancing Asian monsoon rainfall by favoring upper-level divergence over the Bay of Bengal.^[8] Vertical structure studies using empirical orthogonal functions reveal two dominant variability modes: one tied to zonal shifts and another to meridional expansions, influencing tropical cyclone genesis over the western North Pacific by modulating shear.^[9]^[28] These findings, drawn from ERA5 reanalyses and radiosonde networks, underscore the TEJ's evolving role in teleconnections amid observed climatic shifts.^[27]

Interactions with Monsoon Systems

Link to Asian Summer Monsoon

The Tropical Easterly Jet (TEJ), a zonally oriented upper-tropospheric easterly wind maximum at approximately 100–150 hPa over the Indian peninsula and extending westward, forms as an integral component of the Asian summer monsoon circulation during boreal summer (June–September). It arises from the intense diabatic heating over the Tibetan Plateau and surrounding Asian landmasses, which establishes a reversed north-south temperature gradient in the upper troposphere—cooler air over the plateau relative to the warmer tropics—driving easterly thermal winds via geostrophic balance.^[2]^[1] This gradient reversal, peaking in July with core speeds of 20–40 m/s at 15°N latitude, sustains the monsoon's vertically sheared structure, linking low-level westerly moisture influx from the Indian Ocean to upper-level outflow.^[8] The TEJ modulates Asian summer monsoon rainfall, particularly over India, by influencing upper-level divergence that enhances convective ascent in the monsoon trough and suppresses it during breaks. Observational analyses reveal a tight positive correlation between TEJ intensity and Indian summer monsoon rainfall (ISMR), where stronger jets (e.g., exceeding 30 m/s) align with above-normal precipitation totals, as the jet's enhanced easterlies promote vertical shear conducive to organized convection and cyclone genesis in the Bay of Bengal.^[23]^[4] Conversely, weakened TEJ states, such as those observed in deficient monsoon years like 2002 and 2009, reduce shear and dynamical support, leading to suppressed rainfall and prolonged breaks.^[29] Interannual variability in TEJ strength and meridional position further ties it to monsoon predictability, with El Niño-Southern Oscillation (ENSO) phases modulating the jet via altered heating patterns; La Niña conditions often amplify TEJ easterlies and ISMR, while El Niño weakens them.^[1] The jet also demarcates the southern boundary of the Asian monsoon anticyclone, channeling transport of monsoon tracers like water vapor and pollutants, thereby influencing regional precipitation efficiency.^[30] Long-term weakening trends in TEJ speed, documented at 0.5–1 m/s per decade since the 1970s, have been associated with declining monsoon vigor, though attribution to anthropogenic forcing remains debated pending further dynamical modeling.^[29]^[31]

Influence on African Monsoon and Sahel Rainfall

The Tropical Easterly Jet (TEJ), a mid-tropospheric easterly flow peaking at around 200 hPa over West Africa during boreal summer, positively correlates with Sahel rainfall on interannual and decadal timescales, with stronger jet intensities linked to higher precipitation totals in the region (10°–20°N, 15°W–20°E).^[32] This association arises primarily from the TEJ's modulation of upper-level divergence, which enhances vertical motion and favors the development of mesoscale convective systems (MCSs) responsible for much of the Sahel's intense rainfall events.^[13] Observations from reanalysis datasets spanning 1979–2018 confirm this linkage, showing that TEJ maxima coincide with periods of increased convective activity over the Sahel, independent of large-scale moisture transport alone.^[33] On intraseasonal and synoptic scales, TEJ fluctuations drive short-term rainfall variability by altering the propagation of African easterly waves (AEWs), which initiate squall lines and thunderstorms; a intensified TEJ promotes upper-tropospheric outflow that sustains these systems, leading to rainfall surges of up to 20–50 mm day⁻¹ in active phases.^[32] In wet monsoon years, the TEJ strengthens relative to climatology (exceeding 20 m s⁻¹ in core speeds), often coupling with a weakened and northward-shifted African Easterly Jet (AEJ) at 600–700 hPa, which reduces shear and enhances instability for convection.^[34] This dynamic interplay contributes to zonal rainfall gradients, with enhanced precipitation over the central Sahel during strong TEJ episodes.^[1] Reanalysis products like ERA-Interim and MERRA-2 depict consistent TEJ-Sahel rainfall correlations (r ≈ 0.4–0.6 for July–September averages over 1980–2010), though discrepancies in jet position and intensity across datasets (e.g., weaker TEJ in CFSR) underscore uncertainties in quantifying exact causal strength without satellite validation.^[13] Model simulations from 1983–2014 further reveal that TEJ core strength significantly correlates with convective (but not large-scale) Sahel rainfall during July–August–September, implying the jet's primary role in amplifying localized extremes rather than mean fields.^[33] These patterns persist in empirical reconstructions, where TEJ variability explains up to 30% of interannual Sahel precipitation anomalies when integrated with sea surface temperature influences.^[35]

Variability and Observed Changes

Interannual and Decadal Fluctuations

The Tropical Easterly Jet (TEJ) displays pronounced interannual variability, primarily driven by the El Niño-Southern Oscillation (ENSO). During El Niño phases, characterized by warm sea surface temperatures in the eastern equatorial Pacific, the TEJ weakens significantly at upper tropospheric levels (around 200 hPa), often coinciding with reduced divergent kinetic energy flux and eastward shifts in tropical circulation patterns.^[36] This attenuation is linked to suppressed low-level monsoon westerlies over the Indian Ocean and diminished rainfall over the Indian subcontinent, as observed in data from 1965–1982.^[36] Conversely, La Niña conditions tend to strengthen the jet, enhancing upper-level divergence over equatorial Africa and supporting robust monsoon convection.^[36] Empirical orthogonal function (EOF) analysis of the TEJ's vertical structure (300–70 hPa) identifies the leading mode (EOF1) as capturing uniform zonal wind anomalies indicative of overall intensification or weakening, with interannual fluctuations strongly modulated by ENSO indices.^[9] This mode reflects coherent changes across the troposphere, tied to large-scale tropical divergent circulations that amplify or dampen jet core speeds by up to 5–10 m/s in extreme ENSO years.^[9] A secondary mode (EOF2) exhibits out-of-phase anomalies between the upper troposphere and lower stratosphere, operating on quasi-biennial timescales and influenced by the Quasi-Biennial Oscillation (QBO), which indirectly affects convection over the tropical Indian Ocean.^[9] On decadal timescales, the TEJ exhibits interdecadal fluctuations superimposed on interannual signals, with EOF1 variability linked to basin-scale ocean modes such as the Atlantic Multidecadal Oscillation (AMO) and Pacific Decadal Oscillation (PDO).^[9] These oscillations contribute to prolonged strengthening or weakening phases, altering jet intensity by influencing persistent sea surface temperature gradients and meridional temperature contrasts in the upper troposphere.^[9] Regime shifts in TEJ-monsoon rainfall correlations have been documented around the early 1990s and early 2000s, attributed to enhanced variability in tropical eastern Indian Ocean precipitation that disrupts traditional linkages.^[23] Such decadal changes manifest in altered frequencies of TEJ core location modes, with implications for redistributed upper-level divergence and regional monsoon precipitation patterns.^[8]

Long-Term Trends Including Weakening

Observational reanalyses consistently document a multi-decadal weakening of the Tropical Easterly Jet (TEJ) during the Asian summer monsoon season, with strength reductions evident across pressure levels from the upper troposphere downward. Analysis of NCEP-NCAR reanalysis data from 1950 to 2009 shows a significant decline, including a 5 m s⁻¹ decrease in thermal wind shear over the 300–150 hPa layer and the disappearance of the 30 m s⁻¹ wind speed contour by the 2000–2009 decade, indicating diminished jet intensity and vertical extent.^[11] This trend arises from a diminished upper-tropospheric meridional temperature gradient, driven by 0.5°C warming over the equatorial Indian Ocean—linked to enhanced convection from sea surface temperature rises of 0.8–1.2°C—and 1°C cooling over the Tibetan anticyclone region, yielding a net gradient reduction of approximately 1.5°C and consequent weakening of the easterly thermal wind.^[11] Extending to 1948–2011 using the same reanalysis dataset, the TEJ core speeds declined notably, from 25 m s⁻¹ to 20 m s⁻¹ at 100 hPa and from 30 m s⁻¹ to 25 m s⁻¹ at 150 hPa, with maximum zonal wind decreases of 8 m s⁻¹ at 100 hPa over the equatorial Indian Ocean, 7 m s⁻¹ at 150 hPa in the southwest Indian Ocean, and 4 m s⁻¹ at 200 hPa, alongside reduced horizontal extent.^[31] A key precursor is the reduced land–sea temperature contrast in May, correlating positively with TEJ strength (r = 0.52–0.64 across levels), which hampers jet development; El Niño events further contribute by suppressing the gradient.^[31] Shorter-period observations from 1995–2014 corroborate the pattern, recording a mean TEJ intensity drop of 8.1 m s⁻¹ overall, with larger declines over the Indian Ocean (17.9 m s⁻¹) and eastern Pacific (6.8 m s⁻¹) sectors.^[26] Such trends align with broader weakening of upper-level monsoon circulation, though reanalysis products like NCEP-NCAR may introduce minor artifacts from assimilation biases, as cross-verified in peer-reviewed evaluations.^[11]^[26] Projections from CMIP6 models, evaluated against these observations (which models underestimate by 22% in intensity), forecast amplified weakening—11% in mean intensity and 6% in spatial extent by 2081–2100 under SSP5-8.5—extrapolating observed drivers like El Niño-like warming patterns but with uncertainties in simulating historical gradients.^[26]

Impacts on Weather Patterns

Effects on Tropical Cyclone Activity

The Tropical Easterly Jet (TEJ) primarily exerts a suppressive influence on tropical cyclone (TC) activity in the North Indian Ocean through the generation of strong vertical wind shear during the boreal summer monsoon season. Upper-level easterly winds associated with the TEJ, peaking at 200 hPa altitudes, create differential velocities between surface westerlies (or light winds) and upper-tropospheric easterlies, exceeding 15-20 m/s in many cases, which disrupts vortex organization and inhibits TC genesis and intensification from July to September.^[37] This shear mechanism is most pronounced over the Bay of Bengal and Arabian Sea, where the TEJ's core aligns with monsoon heating maxima, limiting TC formation to pre-monsoon (May-June) and post-monsoon (October-November) periods when shear is reduced.^[4] Interannual variability in TEJ strength modulates this suppression, with weaker jets correlating to reduced shear and enhanced TC potential intensity. A decreasing TEJ trend observed since the 1970s—attributed to factors like altered Tibetan Plateau heating—has been linked to lower shear thresholds, enabling cyclones to reach higher maximum sustained winds; modeling shows that a 10% TEJ weakening could increase TC central pressures by up to 10 hPa less, fostering category 4-5 equivalents in the basin.^[37] High-frequency TEJ fluctuations, particularly in June, further alleviate mean shear inhibition in the Bay of Bengal, promoting 20-30% more frequent genesis events and intensities during transitional monsoon onset phases, as easterly momentum divergences create localized low-shear windows.^[4] In the western North Pacific, the TEJ's entrance region dynamics exhibit an opposite effect, where intensified jet streams enhance TC genesis through convergence-induced vorticity and moisture influx. Correlation analyses from 1979-2018 reanalyses reveal a positive relationship (r ≈ 0.4-0.6) between TEJ core speeds exceeding 25 m/s at 15-20°N and annual TC counts, with stronger jets favoring 10-15 additional systems via amplified easterly wave activity.^[28] This regional contrast underscores the TEJ's causal role via shear modulation and wave-train interactions, though empirical attribution remains challenged by coupled ocean-atmosphere feedbacks.^[28]

Teleconnections to Regional Precipitation

The Tropical Easterly Jet (TEJ) exhibits teleconnections to precipitation in regions outside its primary domain over the tropical Indian Ocean and Africa, primarily through modulation of upper-level divergence, jet interactions, and coupling with large-scale modes like ENSO. These links often involve lagged responses where TEJ intensity alters vertical motion and wave propagation, influencing convective activity remotely. For instance, a strengthened TEJ enhances upper-tropospheric diffluence, which can propagate anomalies via Rossby wave trains or meridional circulation adjustments.^[38] In eastern Africa, the TEJ mediates the ENSO teleconnection to summer rainfall, with a robust positive correlation between TEJ strength and precipitation during El Niño years in observations from 1979–2014. Global climate models that accurately represent the TEJ's vertical structure better simulate this linkage, attributing it to TEJ-induced changes in the Walker circulation that amplify moisture convergence over East Africa; model biases in TEJ position lead to underestimated rainfall responses, with correlations exceeding 0.5 in high-fidelity simulations.^[38] Further teleconnections extend to the Arctic, where intensified TEJ during boreal summer correlates with positive precipitation anomalies, explaining 17.6% of variance in Arctic-wide summer rainfall from 1979–2020 data. This association arises via a northward-shifted Asian westerly jet and enhanced Indian monsoon circulation, which increase baroclinicity and mid-tropospheric cold anomalies over the Arctic, fostering moisture convergence; numerical sensitivity experiments confirm causality, showing TEJ-driven tropical heating propagates poleward through strengthened zonal flows.^[39] Intraseasonally, a strong TEJ synchronizes extreme rainfall events between northern India and the Sahel, with a 2–3 day lag observed in events from 2019–2023, driven by boreal summer intraseasonal oscillations under La Niña conditions. This pattern features TEJ enhancement over India leading to upper-level diffluence that favors convective outbreaks in West Africa, with correlations peaking at r=0.4–0.6 for daily precipitation extremes exceeding the 95th percentile.^[40] In Sudan, historical analyses from 1958–1988 link TEJ core position and speed to interannual rainfall variability, with southerly TEJ shifts associated with 10–20% higher seasonal totals due to augmented easterly momentum flux enhancing low-level convergence.^[24]

Debates on Causes and Attribution

Natural Variability Factors

The interannual variability of the Tropical Easterly Jet (TEJ) is predominantly influenced by the El Niño-Southern Oscillation (ENSO), with the jet typically weakening during El Niño warm events and strengthening during La Niña cool phases.^[36] This relationship arises from ENSO-modulated convection over the Indian subcontinent and adjacent oceans, where suppressed heating during El Niño reduces the meridional temperature gradient that sustains the jet's easterly momentum.^[41] Observations from 1958 to 1985 indicate that TEJ core speeds at 200 hPa over South Asia average 5-10 m/s weaker in El Niño summers compared to La Niña years, correlating with reduced monsoon rainfall.^[42] The Indian Ocean Dipole (IOD) contributes to TEJ fluctuations through its impact on regional sea surface temperatures and atmospheric circulation, with positive IOD phases often enhancing easterly anomalies via strengthened Walker circulation.^[10] Lag correlations between prior-season IOD indices and boreal summer TEJ intensity reveal statistically significant links, where positive IOD events precede stronger jets by promoting anomalous subsidence over the western Indian Ocean.^[10] Combined with ENSO, IOD explains up to 30-40% of TEJ interannual variance in reanalysis data, though its isolated effect diminishes in neutral ENSO years.^[41] Stratospheric influences, particularly the Quasi-Biennial Oscillation (QBO), modulate TEJ strength on subseasonal to interannual scales, with westerly QBO phases associated with enhanced jet speeds and easterly phases linked to weakening.^[43] This occurs via QBO-induced changes in tropical tropopause stability and vertical wind shear, which alter upper-tropospheric momentum transport; composite analyses show TEJ maxima 3-5 m/s higher during westerly QBO compared to easterly phases in ERA5 reanalyses from 1979-2020.^[43] While less dominant than ENSO for year-to-year shifts, QBO-TEJ coupling amplifies variability during monsoon onset, independent of surface ocean forcing.^[44]

Anthropogenic Climate Influence and Empirical Evidence

Observational analyses of reanalysis data from 1979 to 2012 reveal a progressive weakening in the intensity and areal extent of the Tropical Easterly Jet (TEJ), with wind speeds in the core declining by approximately 1-2 m/s per decade.^[11] This trend aligns temporally with anthropogenic greenhouse gas emissions driving global surface warming, which has reduced pre-monsoon land-sea temperature contrasts over Asia by enhancing continental heating relative to oceans.^[31] However, such correlations do not establish causation, as interannual fluctuations tied to natural modes like El Niño-Southern Oscillation (ENSO) and Indian Ocean Dipole explain much of the short-term variance in TEJ strength, complicating direct attribution.^[1] Empirical attribution studies specifically isolating anthropogenic signals in the TEJ remain scarce, with most evidence derived from process-oriented modeling rather than formal detection-attribution frameworks applied to observations. Climate models from the CMIP6 ensemble, forced by historical and projected greenhouse gas concentrations, simulate a mean TEJ intensity reduction of about 11% and a 6% contraction in spatial extent by the end of the 21st century under high-emission scenarios, linked mechanistically to tropospheric stabilization from enhanced moist static energy and diminished upper-level easterly shear.^[26] These projections hinge on amplified tropical upper-tropospheric warming outpacing surface trends, potentially cooling the tropopause over heated landmasses like Asia, though observational confirmation of this differential warming's role in TEJ dynamics is indirect and confounded by sparse upper-air data over the region.^[45] Sensitivity experiments indicate that TEJ responses vary with spatial patterns of anthropogenic warming, such as faster Arctic versus tropical amplification, which could either reinforce or mitigate jet weakening through altered meridional temperature gradients and Hadley cell expansion.^[46] Observational proxies, including satellite-derived outgoing longwave radiation and radiosonde winds, support a broad tropical circulation slowdown concurrent with global warming, but TEJ-specific signals are statistically marginal after accounting for aerosol effects and internal variability.^[11] Absent longer-term paleoclimate analogs or advanced fingerprinting techniques, anthropogenic influence on the TEJ is inferred primarily from model consensus rather than robust empirical detection in the 40-year instrumental record.

Modeling and Projections

Representation in Climate Models

Most general circulation models (GCMs) simulate the Tropical Easterly Jet (TEJ) as a dynamically induced upper-tropospheric easterly flow, peaking at 100–150 hPa during boreal summer, arising from thermal contrasts between heated continental landmasses and cooler oceans that establish meridional temperature gradients and drive the return branch of the Hadley cell.^[26] In the Coupled Model Intercomparison Project Phase 6 (CMIP6) ensemble, the majority of models reproduce the basic climatology, seasonal evolution from May to September, and interannual variability of both the Indian Ocean (IO-TEJ) and eastern Pacific (EP-TEJ) branches, capturing their easterly cores near 10°–15°N.^[26] However, substantial inter-model diversity persists, with individual models showing biases in jet position, meridional extent, and maximum speeds exceeding 6 m s⁻¹ in the cores over the IO and EP regions.^[26] The multi-model mean often exhibits a westerly bias, reflecting underestimated easterly wind intensities compared to reanalysis data such as ERA-Interim, which may stem from deficiencies in parameterizing tropical convection, land-sea heating contrasts, or coupled ocean-atmosphere interactions.^[47] Earlier atmospheric GCM studies, including those examining monsoon contrasts, have similarly demonstrated reasonable simulation of TEJ intensity variations tied to Tibetan Plateau heating and upper-level divergence, though with analogous underestimations during strong monsoon years.^[48] These representational challenges contribute to uncertainties in modeling TEJ responses to external forcings.^[26]

Projected Changes and Uncertainties

Climate models from the Coupled Model Intercomparison Project Phase 6 (CMIP6) project a substantial weakening of the Tropical Easterly Jet (TEJ) under future warming scenarios, with the mean intensity decreasing by approximately 11% and its spatial extent contracting by about 6% by the end of the 21st century under the SSP2-4.5 emissions pathway.^[26] This projected decline is attributed to enhanced atmospheric stability and reduced meridional temperature gradients in the tropics, which diminish the thermal forcing that drives the jet's easterly winds during boreal summer.^[26] Such changes align with broader expectations of a weakened upper-level monsoon circulation over South Asia, as indicated by simulations of the South Asian Summer Monsoon (SASM), where the TEJ serves as a key dynamical feature.^[49] Projections vary with spatial patterns of global warming; for instance, a La Niña-like equatorial Pacific warming pattern is simulated to strengthen the TEJ over the western Pacific while weakening it over the Indian Ocean, potentially altering regional divergence and convergence patterns.^[46] Conversely, El Niño-like warming yields the opposite response, with overall TEJ intensification over the Indian Ocean sector.^[46] Post-2100 projections under high-emissions scenarios suggest even more pronounced weakening, driven by rapid tropical tropospheric warming that increases static stability and suppresses vertical motion.^[50] Uncertainties in these projections stem primarily from inter-model differences in simulating tropical east Pacific (EP) sea surface temperature warming, which influences the TEJ's thermal wind balance and meridional shear.^[26] CMIP6 models exhibit biases in historical TEJ representation, including underestimation of its intensity and vertical structure over Africa and Asia, which may propagate into future simulations and amplify spread in projected changes.^[13] Additionally, the sensitivity of TEJ response to aerosol forcing and internal variability, such as ENSO teleconnections, introduces further ambiguity, as decadal prediction models show limited skill in forecasting TEJ anomalies beyond a few years.^[51] These factors underscore the need for improved model physics, particularly in resolving upper-tropospheric dynamics and convective processes that sustain the jet.^[52]

References

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Characteristics and Mechanisms of the Interannual Variability of the ...
The tropical easterly jet (TEJ) is a prominent upper-level circulation in the tropics and an essential component of the Asian summer monsoon system ( ...
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Frequently Asked Questions (FAQs) on Monsoon - IMD Pune
... jet stream centred near about the latitude of Chennai at 150 hPa in July. This is Tropical easterly jet. The jet stream runs from the east coast of Vietnam ...<|separator|>
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Jet Streams
Also peculiar to the tropical latitudes of the Northern Hemisphere is a high-level jet called the tropical easterly jet stream. Such jets are located about ...
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During the peak of the monsoon season, the TEJ generally exceeds 35 m s−1 (Nicholson et al. 2007), which is the cause of a strong vertical easterly shear over ...
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Mar 13, 2024 · A noticeable feature in the UT is the tropical easterly jet (TEJ) streams with speeds often exceeding 30 m/s which span around the equator ...
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Oct 6, 2009 · [10] The TEJ is an intense narrow horizontal current of air associated with strong vertical wind shear. According to World Meteorological ...
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Jun 17, 2024 · The upper-tropospheric tropical easterly jet (TEJ) is one of the most important systems in modulating the Asian summer monsoon rainfall.
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The upper-level tropical easterly jet accelerates over the Arabian Sea during and after Pacific La Nina and the cool-west Indian Ocean dipole, and shows four ...
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Because of the low Coriolis force over the TEJ region (A), a small change in the temperature gradient and the consequent change in thermal wind can cause large ...
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Aug 11, 2025 · The southeastern Tibetan Plateau heating significantly influences the tropical easterly jet in its inflow region in the interannual time scale.
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Apr 30, 2020 · This paper compares the characteristics of the Tropical Easterly Jet (TEJ) and upper-level winds in six reanalysis products, compares them with soundings at ...<|control11|><|separator|>
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[PDF] RR-006 - Indian Institute of Tropical Meteorology
Sep 30, 1972 · Tibetan Plateau and also for the development of tropical easterly jet. ... sensible heat or latent heat to the presence of the anticyclone ...
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[18]
(PDF) The Impact of Orography and Latent Heating on the Location ...
Feb 5, 2017 · Orography was found to have minimal impact on the simulated TEJ hence indicating that latent heating is the crucial parameter. The primacy of ...
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Because orography hardly impacted the TEJ in the previous simulations, it is instructive to study the atmospheric response only due to heating. The multiplicity ...
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[PDF] nimbus 3 satellite observations of,ozone associated with the easterly
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Correspondingly, the projected mean easterly wind and extent decrease by about 11% and 6%, respectively, implying a general weakening of the tropical upper- ...Missing: altitude | Show results with:altitude<|control11|><|separator|>
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[33]
Sahel rainfall strength and onset improvements due to more realistic ...
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[34]
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Dramatic Weakening of the Tropical Easterly Jet Projected by CMIP6 ...
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Substantial shift in phase and amplitude of Indian rainfall beyond 2100
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Decadal prediction, often termed "near-term climate prediction", represents a growing area of research within climate prediction and climate change studies, ...
[52]
How do coupled models represent the African Easterly Jets and their ...
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