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New metrics and evidence are presented that support a linkage between rapid Arctic warming, relative to Northern hemisphere mid-latitudes, and more frequent high-amplitude (wavy) jet-stream configurations that favor persistent weather patterns. We find robust relationships among seasonal and regional patterns of weaker poleward thickness gradients, weaker zonal upper-level winds, and a more meridional flow direction. These results suggest that as the Arctic continues to warm faster than elsewhere in response to rising greenhouse-gas concentrations, the frequency of extreme weather events caused by persistent jet-stream patterns will increase.
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Environ. Res. Lett. 10 (2015) 014005 doi:10.1088/1748-9326/10/1/014005
LETTER
Evidence for a wavier jet stream in response to rapid Arctic warming
Jennifer A Francis
1
and Stephen J Vavrus
2
1
Institute of Marine and Coastal Sciences, Rutgers University, New Brunswick, New Jersey, USA
2
Center for Climatic Research, University of Wisconsin-Madison, Madison, Wisconsin, USA
E-mail: francis@imcs.rutgers.edu
Keywords: jet stream, Arctic amplication, extreme weather
Abstract
New metrics and evidence are presented that support a linkage between rapid Arctic warming, relative
to Northern hemisphere mid-latitudes, and more frequent high-amplitude (wavy) jet-stream cong-
urations that favor persistent weather patterns. We nd robust relationships among seasonal and
regional patterns of weaker poleward thickness gradients, weaker zonal upper-level winds, and a more
meridional ow direction. These results suggest that as the Arctic continues to warm faster than else-
where in response to rising greenhouse-gas concentrations, the frequency of extreme weather events
caused by persistent jet-stream patterns will increase.
This paper builds on the proposed linkage between
Arctic amplication (AA)dened here as the
enhanced sensitivity of Arctic temperature change
relative to mid-latitude regionsand changes in the
large-scale, upper-level ow in mid-latitudes [1,2].
Widespread Arctic change continues to intensify, as
evidenced by continued loss of Arctic sea ice [3];
decreasing mass of Greenlands ice sheet [4], rapid
decline of snow cover on Northern hemisphere
continents during early summer [5], and the contin-
ued rapid warming of the Arctic relative to mid-
latitudes. While these events are driven by AA, they
also amplify it: melting ice and snow expose the dark
surfaces beneath, which reduces the surface albedo,
further enhances the absorption of insolation, and
exacerbates melting. Expanding ice-free areas in the
Arctic Ocean also lead to additional evaporation that
augments warming and Arctic precipitation [6].
Traditionally AA is measured as the change in sur-
face air temperature in the Arctic relative to either the
Northern hemisphere or the globe [7]. It arises owing
to a variety of factors, including the loss of sea-ice and
snow, increased water vapor, a thinner and more frac-
tured ice cover, and differences between the Arctic and
lower latitudes in the behavior of lapse-rate and radia-
tive feedbacks [813]. Here we do not address the rela-
tive importance of various factors causing AA, but it is
clear from the height-latitude anomalies of air tem-
perature, geopotential, and zonal wind (gure 1) that
AA results in large part from near-surface heating,
although contributions from poleward heat transport
may also play a role [14].
Seasonal time series and trends in AA based on two
metrics and varying initial years are presented in
gure 2. The more traditional method of assessing AA
is to subtract changes in near-surface (1000 hPa) air
temperature anomalies in mid-latitudes (6030°N)
from those in the Arctic (left side of gure 2). A posi-
tive value of AA indicates that the Arctic is warming
faster than mid-latitudes. Both the time series and
progressive 15 year trends (gure 2, bottom) indicate
an increasingly positive AA in all seasons, particularly
in fall and winter, in agreement with previous analyses
[8]. Starting in the 1990s, coincident with an acceler-
ated decline in Arctic sea-ice extent [3], AA values and
trends became positive in all four seasons for the rst
time since the beginning of the modern data record in
the late 1940s, illustrating the Arctics enhanced sensi-
tivity to global warming.
The right side of gure 2presents an alternative
metric for AA based on the difference in the
1000500 hPa thickness change in the Arctic relative
to that in mid-latitudes (same zones as for the tradi-
tional method). Arguably the thickness difference is
more relevant for assessing the effects of AA on the
large-scale circulation, as it represents differences in
warming over a deeper layer of the atmosphere that
should more directly inuence winds at upper levels.
Several recent autumns have exhibited strong warm-
ing anomalies in some mid-latitude areas, contribut-
ing to the weakened positive trend after 2007. It is
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important to note the recent emergence of the signal of
AA from the noise of natural variability: since 1995
near the surface and since 2000 in the lower tropo-
sphere. This short period presents a substantial chal-
lenge to the detection of robust signals of atmospheric
response amid the noise of natural variability [15,16].
Thus for this study we dene the period from 1995 to
2013 as the AA era.While this demarcation is con-
sistent with previous studies [17], we also investigate
the effects of choosing different commencement years
on detecting changes in the frequency of high-ampli-
tude jet-stream congurations.
Figure 1. Annual-mean anomalies in air temperature (left), geopotential (middle), and zonal winds (right) during 19952013 relative
to 19812010 for 4080°N and 1000250 hPa. Data were obtained from the NCEP/NCAR Reanalysis at http://www.esrl.noaa.gov/
psd/.
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Environ. Res. Lett. 10 (2015) 014005 J A Francis and S J Vavrus
The following linkage between AA and mid-lati-
tude weather patterns has been hypothesized [1].
Increasing AA weakens the poleward temperature
gradienta fundamental driver of zonal winds in
upper levels of the atmospherewhich causes zonal
winds to decrease, following the thermal wind rela-
tionship [18]. A weaker poleward temperature gra-
dient is also a signature of the negative phase of the
so-called Arctic oscillation/Northern annular mode
(AO/NAM), in which weaker zonal winds are asso-
ciated with a tendency for a more meridional ow,
blocking, and a variety of extreme weather events in
much of the extratropics [19]. Disproportionate
Arctic warming and sea-ice loss favor a negative
AO/NAM aloft [1,2,20,21] and a Northward
migration of ridges in the upper-level ow [1], fur-
ther contributing to an increased meridional pat-
tern. As the wave amplitude and/or frequency of
amplied ow regimes increases, the incidence of
blocking becomes more likely [2], which reduces
the Eastward propagation speed of the pattern.
Consequently, the associated weather systems per-
sist longer in a particular area. Extreme weather
events caused by prolonged weather conditions
(such as cold spells, stormy periods, heat waves, and
droughts), therefore, should also become more
likely, as illustrated by recent studies linking these
events to high-amplitude planetary waves [2224].
Because AA is strongest in fall and winter
(gure 2), the atmospheric response is expected to be
largest and observed rst in these seasons. Results cor-
roborate this expectation [1], showing a marked
reduction in the poleward thickness gradient and
weaker zonal winds at 500 hPa during fall (OND) and
winter (JFM) since 1979 over the North America/
North Atlantic study region. Others nd statistically
signicant decreases in zonal-mean zonal winds in the
fall but not in winter [15].
Marked spatial and seasonal variability in the
changing poleward thickness gradient dictates pat-
terns of change in zonal winds. While hemisphere-
mean, mid-latitude, zonal winds at 500 hPa have
decreased by about 10% since 1979 during fall [23], no
robust hemispheric trends are apparent in other sea-
sons owing to the spatial variability of the AA signal.
The objectives of the present study are to examine
regional and seasonal expressions of AA that produce
changes in poleward thickness gradients, correspond-
ing effects on zonal wind speeds, and the hypothesized
increase in highly amplied jet-stream regimes.
Recent studies have presented a mixed picture regard-
ing this atmospheric response to AA. Some observa-
tional analyses nd evidence of increased wave
amplitude in certain locations and seasons, but statis-
tical signicance is often lacking [1,15,16], likely
owing to the recent emergence of AA from natural
Figure 2. Arctic amplication seasonal time series (a), (b) and trends (c), (d) based on two metrics: (left) differences in 1000 hPa
temperature anomalies (relative to 19482013 mean, °C) between the Arctic (7090°N) and mid-latitudes (3060°N); (right)
differences in 1000500 hPathickness anomalies (percentof meanfor eachzone) betweenthe twozones. Contoured colorsin c,d
indicate moving 15 year trends (C/decade for T1000 and percent of mean per decade) for each season. Thex-axis indicatesthe ending
year of each 15 year period between 1949 and 2013, and asterisks indicate ending year of periods with signicant trends (condence
>95%, assessed using an F-test goodness of t). Data were obtained from the NCEP/NCAR Reanalysis at http://www.esrl.noaa.gov/
psd/.
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Environ. Res. Lett. 10 (2015) 014005 J A Francis and S J Vavrus
variability. Analyses based on climate model simula-
tions are challenged by the sometimes unrealistic
representations of complex Arctic physics and non-
linear atmospheric dynamics. Nevertheless, they, too,
suggest a more meridional ow (often resembling the
negative phase of the AO/NAM) in response to sea-ice
loss [25], and none suggests that the ow will become
more zonal or that planetary waves will decrease in
amplitude. Measuring changes in the strength of the
zonal wind is straightforward, whereas quantifying the
wavinessof the circulation is not. We therefore aim
to shed further light on this critical aspect of the link-
age by using new techniques to measure the waviness
of the upper-level ow, and we also comment on the
results of previous efforts to diagnose changes in wave
amplitude.
Seasons are dened as follows: winter (JFM),
spring (AMJ), summer (JAS), and fall (OND). These
denitions are selected to coincide with the summer
minimum and winter maximum of Arctic sea-ice
extent, as well as the onset times of freeze and melt. All
data are from the NCEP/NCAR Reanalysis (NRA)
[26] obtained at http://www.esrl.noaa.gov/psd/.
Analysis of 500 hPa height contours
A simple new method was introduced to assess the
daily meridional amplitude of waves in the upper-level
ow [1]. A single contour in the 500 hPa height eld
was selected based on its climatological position within
the strongest gradient, thus representing the path of
the polar jet stream on any individual day. The
planetary wave locations and shapes depicted by height
elds at 500 hPa and those at typical heights of the jet
stream maximum (250 hPa) are very similar. The
selected heights of individual contours vary slightly
with season to match climatological jet-stream loca-
tions: within 50 m of 5600 m during the cool/cold
seasons (JFM, AMJ, OND), and 5700 m during
summer months (JAS). Daily height contours are
subsetted from daily mean 500 hPa elds from the
NRA. Correlations of 500 hPa height anomalies
between NRA and either the NCEP Climate Forecast
System Reanalysis or the European Centre for Med-
ium-Range Forecasts Interim values are over 0.99 in all
seasons (not shown), suggesting that mid-tropo-
spheric height elds in NRA are nearly identical to
those of other reanalyses. Small differences in blocking
statistics among various reanalyses have also been
reported [27].
The selection of particular 500 hPa height con-
tours used for analysis of wave amplitude [1] has been
questioned by assertions that the proper contours to
use should be those exhibiting the greatest degree of
waviness [15]. This study reproduced the increased
wave amplitude in the 5600 m contour from 1979 to
2010, but the same analysis based on the contour iden-
tied as the waviest (5300 m) exhibited no increase in
amplitude. As illustrated in gures 3(a) and (b), how-
ever, the mean latitude of the 5300 m contour during
fall (19802011) is nearly 15° of latitude farther North
than the mean latitude of the 5600 m contour. More-
over, its more Northerly position is far from the core
of strongest upper-level winds and thus its location
differs substantially from the path of the jet stream.
Winds well North of the jet are substantially weaker
(gures 3(a) and (c)), consequently is it not surprising
that the ow is wavier. Arguably, the analysis of the
more Northerly 5300 m contour does not capture the
location and evolution of the polar jet stream, while
the 5600 m contour more closely tracks the shape of
planetary waves in the strongest upper-level ow.
Note that the mean latitude of the strongest zonal
500 hPa winds is nearly identical in both the AA era
(gure 3(a)) and in earlier years (gure 3(c)), suggest-
ing that contours used here and previously [1] repre-
sent the jet-stream location throughout the satellite
record (since 1979).
Meridional circulation index (MCI)
A key outstanding question in the proposed linkage
between AA and jet-stream behavior is whether
weakened poleward thickness gradients are causing
the upper-level ow to become wavier. One measure
of ow waviness is the ratio of the meridional (North/
South) wind component to the total wind speed. We
propose a simple metric to assess this characteristic of
the ow: the MCI:
=
+
vv
uv
MCI *,
22
where uand vare the zonal and meridional compo-
nents of the wind. When MCI = 0, the wind is purely
zonal, and when MCI = 1 (1), the ow is from the
South (North). We note that a more meridional ow
can result from either a stronger vand/or weaker u
wind component through simple vector geometry.
Whatever the cause, an increase in |MCI|indicates a
wind vector aligned more NorthSouth and reects a
changed ow direction. The speed of the meridional
(v) wind may not change, as it is associated with East
West temperature gradients, but if the total wind
vector becomes more meridional, then the ow is by
denition wavier. For example, a Northwesterly wind
could shift to a NorthNorthwesterly wind solely
through a reduction of the Westerly wind component.
For this analysis, MCI is calculated from daily 500 hPa
wind components between 20°N and 80°N at each
gridpoint in NCEP Reanalysis elds.
Coincident anomalies in thickness, zonal
winds, and MCI
In an effort to assess the effects of AA on waviness of
upper-level winds, we compare coincident seasonal
4
Environ. Res. Lett. 10 (2015) 014005 J A Francis and S J Vavrus
anomalies during the AA era relative to the period
from 19812010. Anomalies in the 1000500 hPa
thicknesses are presented in the top panels of gures
47. During fall (OND, gure 7(a)), when sea-ice loss
exerts its largest direct impact, the pattern of AA
extends across much of the Central Arctic, while
during spring (AMJ, gure 5(a)) and summer (JAS,
gure 6(a)) the areas of positive thickness differences
occur primarily over high-latitude land, likely in
response to earlier snow melt [5]. In all seasons,
positive thickness differences are evident in the North-
west Atlantic. This substantial regional and seasonal
variability illustrates the challenge in detecting robust
hemispheric-mean atmospheric responses to AA,
resulting in the low statistical signicance reported in
some previous studies [15,16,28].
The middle panels of gures 47present anoma-
lies in zonal wind speeds at 500 hPa corresponding to
anomalies in the poleward gradient of 1000500 hPa
thicknesses (top panels). Anomalies in |MCI|are
shown in the bottom panels. Immediately obvious is
the close association between the spatial patterns of
weakened poleward gradients (regions where positive
anomalies occur Northward of weaker or negative
anomalies) and areas where zonal winds are weaker.
During winter and autumn (gures 4and 7)a
broad area of substantially weakened poleward
gradient is evident across much of the Northern hemi-
sphere mid-latitudes, particularly in the N. Atlantic
and Northern Eurasia. These areas are closely matched
by the spatial pattern of slower zonal winds, as would
be expected according to the thermal wind relation-
ship. Widespread positive anomalies in |MCI|also cor-
respond to these regions. Changes in the meridional
wind speed, however, are not correlated with either
the changes in poleward gradient or zonal winds, sug-
gesting that changes in |MCI|arise mostly because of
changes in the zonal wind speed. These ndings sup-
port the hypothesis that AA causes a more meridional
character to the upper-level wind ow, but this change
is achieved primarily via a reduction in Westerly winds
rather than through an increase in meridional wind
speeds.
Relationships between these variables on a grid-
point-by-gridpoint basis are illustrated in scatterplots
(gure 8). Gridpoints with weaker (stronger) pole-
ward gradients tend to have larger (smaller) |MCI|
values (red scatter-plots), particularly for gridpoints
with the strongest (top decile) total winds, indicative
of the jet stream. In all seasons, robust relationships
between anomalies in the poleward gradient, zonal
winds, and |MCI|are evident. Moreover, in spring,
summer, and fall, the anomaly in 500 hPa zonal winds
accounts for a much larger fraction of the variance in
Figure 3. Zonal-mean zonal winds for fall (OND) from 1995 to 2013 (a) and from 1979 to 1995 (c). Corresponding zonal-mean
geopotential heights for 19792013 are shown in (b). Dotted horizontal lines highlight the 500 hPa level, white dashed vertical lines
indicate the latitude of maximum mean zonal winds at 500 hPa, and yellow dashed lines are the latitude of the waviest 500 hPa
contour, as identied in [15].
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Environ. Res. Lett. 10 (2015) 014005 J A Francis and S J Vavrus
|MCI|than does the anomaly in the meridional wind
component (variance explained by U500 in JFM, AMJ,
JAS, OND = 0.42, 0.33, 0.61, 0.38; by V500 = 0.59,
0.02, 0.07, 0.001), suggesting that weakened zonal
winds due to AA are the main factor driving the more
meridional ow in these seasons. We also note that
correlations between differences in 500 hPa mer-
idional wind speeds with either the differences in pole-
ward thickness gradient or zonal wind speed were
small and insignicant, suggesting that changes in the |
MCI|arise primarily because of changes in zonal wind
speeds.
Extreme wave frequency
One aspect of the proposed linkage [1] that heretofore
has been difcult to assess is whether the amplitude of
planetary waves is increasing in response to strength-
ening AA. An alternative metric that we pursue here is
the frequency of highly amplied jet-stream cong-
urations. Single contours of daily mean 500 hPa height
elds are used to identify extreme wavesin the jet
stream. Representative contours (5600 m ± 50 m,
except 5700 m ± 50 m in JAS) are selected to represent
the streamline of the strongest 500 hPa winds as
discussed previously, and we note that the selected
contours shift little in latitude with time (gure 3).
Data are analyzed in various longitude zones to
identify days in which the difference between the
maximum and minimum latitudes (ridges and
troughs) of the contour within a region exceeds 35° of
latitude. The threshold of 35° was selected to achieve a
frequency of approximately 20 days per season
(20%). Note that individual high-amplitude events,
Figure 4. Anomalies in winter (JFM) (a) 1000500 hPa thickness (m), (b) zonal wind at 500 hPa (m s
1
), and (c) the absolute value of
the MCI during 19952013 relative to 19812010. Data were obtained from NOAA/ESRL at http://www.esrl.noaa.gov/psd/.
6
Environ. Res. Lett. 10 (2015) 014005 J A Francis and S J Vavrus
such as blocks and cut-off lows, often persist for
several days, thus the frequency of events < frequency
of high-amplitude days.
The frequency of occurrence of high-amplitude
days is assessed in each season and for the AA era
(19952013) relative to the pre-AA period
(19791994). We repeat the analysis using two addi-
tional denitions of the AA era19902013 and
20002013to determine the sensitivity of differ-
ences in high-amplitude days to the time period selec-
ted for the AA era. The mean differences in frequency
between these periods for each season and in selected
regions are presented in table 1. Changes in frequency
are expressed as a percentage relative to the pre-AA
period. We also assess the choice of comparative years
by randomly selecting 100 sets of a number of years
from the pre-AA period corresponding to the length of
each AA era, then calculating the standard deviation of
the extreme-wave frequency in each set. Changes in
frequency from the pre-AA period to the AA era that
exceed one (two) standard deviation(s) are indicated
by an underscore (asterisk).
The changes in frequency are predominantly posi-
tive, indicating more frequent occurrences of highly
amplied jet-stream congurations in the AA era. Sea-
sonal and regional variations are generally consistent
with the spatial patterns of anomalies in poleward
thickness gradients shown in gures 47, particularly
the most robust positive trends in extreme waves over
the Atlantic and North American regions. We nd a
statistically signicant negative correlation (Spear-
mans correlation = 0.30, >90% condence)
between the seasonal, regional-mean change in thick-
ness gradient and the change in extreme-wave fre-
quency. The autumn particularly stands out in table 1,
with increases in extreme waves in all of the categories
representing the post-AA period (19952013 and
20002013), as would be expected because fall exhibits
the largest and most regionally consistent signal of AA.
The Atlantic and North American regions also stand
Figure 5. Same as gure 4but for spring (AMJ).
7
Environ. Res. Lett. 10 (2015) 014005 J A Francis and S J Vavrus
out, with increased frequencies in all post-AA cate-
gories. Decreased frequencies during Asian summer
are consistent with recent cooling in North-Central
Asia (gure 6), which strengthens the poleward gra-
dient, drives stronger zonal winds, and results in a
decreased |MCI|. Overall, the pattern of frequency
change is consistent with expectations of a more
amplied jet stream in response to rapid Arctic warm-
ing. Amplied jet-stream patterns are associated with
a variety of extreme weather events (i.e., persistent
heat, cold, wet, and dry) [22], thus an increase in
amplied patterns suggests that these types of extreme
events will become more frequent in the future as AA
continues to intensify in all seasons. These results may
also provide a mechanism to explain observed associa-
tions between sea-ice loss and continental heat waves
[23,29], cold spells [24,30,31], heavy snowfall [2],
and anomalous summer precipitation patterns in Eur-
ope [32].
Discussion and conclusions
The Arctic has warmed at approximately twice the rate
of the Northern mid-latitudes since the 1990s owing to
a variety of positive feedbacks that amplify green-
house-gas-induced global warming. This dispropor-
tionate temperature rise is expected to inuence the
large-scale circulation, perhaps with far-reaching
effects. The North/South temperature gradient is an
important driver of the polar jet stream, thus as rapid
Arctic warming continues, one anticipated effect is a
slowing of upper-level zonal winds. It has been
Figure 6. Same as gure 4but for summer (JAS).
8
Environ. Res. Lett. 10 (2015) 014005 J A Francis and S J Vavrus
hypothesized that these weakened winds would cause
the path of the jet stream to become more meandering,
leading to slower Eastward progression of ridges and
troughs, which increases the likelihood of persistent
weather patterns and, consequently, extreme events
[1]. While weaker zonal winds have been observed in
response to reduced poleward temperature gradients,
the link to a wavier upper-level ow has not yet been
conrmed [31,33], although recent studies provide
strong support of a mechanism linking sea-ice loss in
the Barents/Kara Sea with amplied patterns over
Eurasia during winter [24,34] and summer [23]. We
also note that the annual-mean NOAA-tabulated
climate extreme index for the US [35] has increased by
approximately one-third in the AA era relative to pre-
AA years, though it is presently unknown whether
rapid Arctic warming is a contributing factor.
Here we provide evidence demonstrating that in
areas and seasons in which poleward gradients have
weakened in response to AA, the upper-level ow has
become more meridional, or wavier. Moreover, the
frequency of days with high-amplitude jet-stream
congurations has increased during recent years.
These high-amplitude patterns are known to produce
persistent weather patterns that can lead to extreme
weather events [22,23]. Notable examples of these
types of events include cold, snowy winters in Eastern
North America during winters of 2009/10, 2010/11,
and 2013/14; record-breaking snowfalls in Japan and
SE Alaska during winter 2011/12; and Middle-East
oods in winter 2012/2013, to name only a few.
We assess anomalies in the poleward
1000500 hPa thickness gradient during the AA era
(since the mid-1990s) relative to climatology
(19812010), along with corresponding changes in the
Figure 7. Same as gure 4but for fall (OND).
9
Environ. Res. Lett. 10 (2015) 014005 J A Francis and S J Vavrus
zonal winds at 500 hPa and the waviness of the
500 hPa ow (|MCI|). While these time periods are
short and certainly include effects of other natural
uctuations in the climate system, the conspicuous
emergence of AA since the mid-1990s dictates this
focused temporal analysis to identify responses of the
large-scale circulation to this newforcing. Future
work will analyze climate model projections of a future
with greater global warming and intensied AA. A
recent study [36] documents a reduction in the fre-
quency of atmospheric fronts under strong green-
house forcing, particularly in high latitudes where the
meridional temperature gradient relaxes the most,
suggestive of more persistent weather patterns.
We nd that in all seasons, the regions in which the
poleward gradient weakens also exhibit weaker zonal
winds (as expected via the thermal wind relationship)
and consequently a more meridional, or wavier, ow
character. This localized response is corroborated by
seasonally varying, regional-scale increases in the fre-
quency of amplied jet-stream congurations. The
strongest response occurs during fall, when sea-ice
loss and increased atmospheric water vapor augment
Arctic warming, and a robust response is also evident
during summer over North America and the Atlantic
sectors, when the observed rapid decline of early-sum-
mer snow cover and the lower heat capacity of land
promote a drying and warming of high-latitude land
areas. Signicant increases are observed in winter and
spring, as well. These results reinforce the hypothesis
that a rapidly warming Arctic promotes amplied jet-
stream trajectories, which are known to favor persis-
tent weather patterns and a higher likelihood of
extreme weather events. Based on these results, we
conclude that further strengthening and expansion of
AA in all seasons, as a result of unabated increases in
greenhouse gas emissions, will contribute to an
increasingly wavy character in the upper-level winds,
and consequently, an increase in extreme weather
events that arise from prolonged atmospheric
conditions.
Figure 8. Seasonal scatterplots relating individual gridpoint values of anomalies during 19952013 for zonal and meridional winds at
500 hPa (U500, V500; m s
1
), poleward gradients in 1000500 hPa thickness (m deg
1
), and |MCI|(unitless). Black asterisks indicate
gridpoints corresponding to the highest 10% of total wind speed during 19952013 at 500 hPa, a proxy for the jet stream. Red asterisks
indicate correlations between black points that exceed 50% and p.001.
10
Environ. Res. Lett. 10 (2015) 014005 J A Francis and S J Vavrus
Acknowledgments
The authors are grateful for funding provided by the
National Science Foundations Arctic System Science
Program (NSF/ARCSS 1304097), to programming
assistance from R Kyle Zahn, and for helpful sugges-
tions from Dr John Walsh and two anonymous
reviewers.
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Table 1. Percentage change in seasonal frequency of high-amplitude days from the pre-AA period to the AA-era assessed using three differ-
ent initial years to dene the AA-era: 19902013 (left column under each seasonal heading), 19952013 (middle column), and 20002013
(right column). High-amplitude days are identied when the difference between the maximum and minimum latitude of the selected daily
500 hPa height contour within a specied region exceeds 35° latitude (see text for contour selections). Underlined values indicate changes
that exceed one standard deviation of wave frequencies during the pre-AA period as determined from 100 sets of randomly selected groups
of years of the same number as the corresponding AA era (i.e., 24, 19, and 14 years beginning in 1979). Underlined and asterisked values
exceed two standard deviations.
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Environ. Res. Lett. 10 (2015) 014005 J A Francis and S J Vavrus
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Environ. Res. Lett. 10 (2015) 014005 J A Francis and S J Vavrus
... The reality is that the influence of global climate change on severe storms remains uncertain, so we are "learning as we go," especially when it comes to how upper atmospheric changes may influence storm intensification and trajectories. For example, scientists are just starting to recognize that de-icing of the Arctic Ocean influences the behavior of the jet stream (Francis and Vavrus, 2015), which in turn can influence storm tracks in the northern Gulf of Mexico. ...
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An extensive grid of high-resolution seismic data, hundreds of sediment cores, and a robust radiocarbon-age data set acquired over nearly four decades allows detailed analysis of Holocene coastal evolution of western Louisiana and Texas, USA. Results from this study provide a framework for assessing the response of a myriad of coastal environments to climate change and variable sea-level rise. Climate varies across the region today, spanning four climate zones from humid to semi-arid, and has fluctuated during the Holocene. The most notable changes were alterations between cool/ wet and warm/dry conditions. Sea-level records for the northwestern Gulf of Mexico indicate an average rate of rise during the early Holocene of 4.2 mm/yr, punctuated by rates exceeding 10.0 mm/yr. After ca. 7.0 ka, the rate of rise slowed, and by ca. 4.0 ka, the average rate decreased from 0.6 mm/yr to 0.3 mm/yr. The current rate of sea-level rise in the region is 3.0 mm/yr, marking a return to early Holocene conditions. Despite its incomplete stratigraphic record of coastal evolution during the middle and early Holocene, it is still the most complete record for the Gulf Coast. Bay evolution, as recorded within the offshore Trinity and Sabine incised valleys, was characterized by periods of bayhead delta and tidal delta expansion, followed by episodes of dramatic landward shifts in these environments. The ancestral Brazos, Colorado, and Rio Grande river deltas and coastal barriers also experienced landward stepping during the early Holocene. The widespread nature of these flooding events and their impact on multiple coastal environments suggests that they were caused by episodes of rapid sea-level rise. Similar methods were used to study modern bays, including the acquisition of seismic lines and drill cores along the axes of the bays to examine the magnitudes and timing of transgressive events. Results from Lake Calcasieu, Sabine Lake, Galveston Bay, Matagorda Bay, Copano Bay, Corpus Christi Bay, and Baffin Bay reveal that landward shifts in bayhead deltas, on the order of kilometers per century, occurred between 9.8 ka and 9.5 ka, 8.9–8.5 ka, 8.4–8.0 ka, and 7.9–7.5 ka. These results are consistent with those from offshore studies and indicate that punctuated sea-level rise dominated coastal evolution during the early Holocene. By ca. 7.0 ka, the average rate of sea-level rise in the northern Gulf of Mexico decreased to 1.4 mm/yr, and there was considerable sinuosity of the coastline and variability in the timing of bay and coastal barrier evolution. The diachronous nature of coastal environment migration across the region indicates that sea-level rise played a secondary role to climate-controlled oscillations in river sediment discharge to the coast. At ca. 4.0 ka, the average rate of sea-level rise decreased to 0.5 mm/yr. During this period of slow sea-level rise, coastal bays began to take on their current form, with the exception of changes in the sizes and locations of bayhead deltas caused by changes in sediment supply from rivers. There were also significant changes in the size and configuration of tidal inlets and deltas as a result of barrier growth. The late Holocene was also a time when coastal barriers experienced progradation and transgression on the order of several kilometers. The timing of these changes varied across the region, which is another indication that sea-level rise played a minor role in coastal change during the late Holocene. Instead, barrier evolution during this time was controlled by fluctuations in sand supply to the coast from rivers and offshore sources. Historical records indicate a dramatic reversal in coastal evolution marked by increased landward shoreline migration of chenier plains and coastal barriers across the region. The main cause of this change is accelerated sea-level rise during this century and diminished sediment supply to the coast. Wetlands are also experiencing rapid change due to their inability to keep pace with sea-level rise, especially in areas where subsidence rates are high. Although direct human influence is a factor in these changes, these impacts are more localized. Coastal change is expected to increase over the next several decades as the rate of sea-level rise increases, the climate in Texas becomes more arid, and more severe storms impact the coast.
... In both regions, SAT anomalies were calculated relative to the 1961-1990 climate normal for each month, and then mean annual anomalies were found. This is one of the metrics of Arctic ampli cation (Davy et al. 2018) based on the study by Francis and Vavrus (2015). However, these studies considered single time series of Arctic ampli cation. ...
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The causes of Arctic amplification are widely debated, and a cohesive picture has not been obtained yet. This study has investigated the role of the Atlantic meridional oceanic and atmospheric heat transport into the Arctic in the emergence of Arctic amplification. The integral advective fluxes in the layer of Atlantic waters and in the lower troposphere were considered. The results show a strong coupling between the meridional heat fluxes and regional Arctic amplification in the Eurasian Arctic on the decadal time scales (10–15 years). We argue that the low-frequency variability of Arctic amplification is regulated via the chain of oceanic heat transport – atmospheric heat transport – Arctic amplification. The atmospheric response to the ocean influence occurs with a delay of three years and is attributed to the Bjerknes compensation mechanism. In turn, the atmospheric heat and moisture transport directly affects the magnitude of Arctic amplification, with the latter lagging by one year. Thus, the variability of oceanic heat transport at the southern boundary of the Nordic Seas might be a predictor of the Arctic amplification magnitude over the Eurasian Basin of the Artic Ocean with a lead time of four years. The results are consistent with the concept of the decadal Arctic climate variability expressed via the Arctic Ocean Oscillation index.
... This has implications for claims that the polar jet has become weaker (and wavier) due to a warming Arctic troposphere (Francis & Vavrus, 2015). Our analysis contradicts that view. ...
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Using the ERA5 and JRA-55 reanalysis datasets on latitude bands of nearly equal area, we analyze the trend of 200 mbar zonal wind anomalies for the period 1958-2021 as well as annual-mean latitude of the polar jet stream. We find basically no change of 200 mbar zonal wind in either the JRA-55 or ERA5 dataset. In addition, the polar jet core moves poleward in the Northern Hemisphere, but the movement is not statistically significant, while no poleward shift at all has occurred in the Southern Hemisphere.
... Previous studies addressing the Arctic sea ice anomaly connection with mid-latitude weather have mainly focused on boreal winter and summer by reducing the Arctic-to-mid-latitude thermal gradient (Semenov and Latif 2015;Overland et al. 2016;Peings 2018;Zhang et al. 2020). For example, Francis and Vavrus (2015) believed that a slower eastward progression of Rossby waves due to a weakening poleward temperature gradient could lead to more persistent weather conditions in the Northern Hemisphere mid-latitudes in the summer (Tang et al. 2013a;Coumou et al. 2015). Cohen et al. (2014) pointed out that storm tracks, jet streams, and planetary waves are potential dynamic pathways that link Arctic amplification to midlatitude weather. ...
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This study investigates the association of spring (April–May) Arctic sea ice melt with simultaneous surface air temperature (SAT) over mid-high latitudes of Eurasia from 1979 to 2019 by using observational datasets and simulation experiments. The results show that spring SAT anomalies associated with Arctic sea ice melt display a dipole pattern over Eurasia. A high Arctic sea ice melt corresponds to positive SAT anomalies over northern Eurasia and negative SAT anomalies over most of Asia. The 500 hPa geopotential height anomalies exhibit a wave train structure, and a dominant positive center is located over the Ural Mountains with two negative centers over East Asia and western Europe. This atmospheric circulation anomaly differs from the traditional Eurasian pattern and the North Atlantic-Eurasian teleconnection pattern due to their different spatial modes. Simulation experiments forced by Arctic sea ice anomalies reproduce the major characteristics of observational associations. Observations and numerical simulations indicate that high Arctic sea ice melt years are often associated with heavy sea ice in winter-spring, which is favorable for the occurrence of Arctic anticyclonic circulation anomaly and lead to a positive SAT anomaly in the Arctic. The Arctic warming not only strengthens polar zonal westerly winds by increasing local baroclinicity, but also weakens zonal winds in mid-latitude through a reduction meridional temperature gradient. It may contribute to the Arctic anticyclonic anomalies enhancement, and then induces a wave train southeastward propagating into the mid-low latitudes. This configuration of atmospheric circulation anomalies provides favorable conditions for the SAT variations over Eurasia.
... Evidence suggests that late winter (JFM), especially during recent decades (sincẽ 1990), featured amplified tropospheric ridge-trough longwave circulation patterns over North America [1,2]. Cold events (daily temperature anomaly <−1.0 standard deviation) in eastern North America usually correspond to an enhanced western ridge/eastern trough jet-stream pattern [3]. ...
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The jet stream over North America alternates between a more zonal direction and a wavy pattern (a more meridional flow) associated with persistent blocking patterns. To better understand these important patterns, we base our study on the frequency of winter (November–February) events during 1981–2020, based on four circulation regime types: blocking, the Alaskan Ridge, North American Ridge/Pacific Wave-Train; and zonal, the Pacific Trough and the central Pacific High/Arctic Low (Amini and Straus 2019). Increased information on within and between season variability is important, as the impacts of blocking include the California heatwave and mid-continent or east coast cold spells. Rather than extensive pattern duration or significant trends, temporal variability is the major feature. In some years the combination of the Alaskan Ridge and North American Ridge/Pacific Wave-Train patterns represent ~5 major events covering 35 days of the 120-day winter period, with individual events lasting 10 days. Within-season multiple occurrences and short durations dominate the winter meteorology of the continental United States. The characterization of the persistence of these blocking events is relevant for extended range forecasts.
... Concurrently, meridional wind component show an increasing trend over this region for the same time-period than zonal wind component (Supplementary Fig. S4). Recent studies have reported the pole-ward migration of atmospheric flow in the Northern Hemisphere during fall and winter 39,40 . Thus, it is likely that increase in moisture availability in combination with a meridional intensification of the flow pattern during recent decades support the increase in ARs frequency along the west coast of India. ...
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Indo-Gangetic Plains (IGP) experiences persistent and widespread rise of fog and haze during the winter season. This has been attributed to the rise in pollution levels and water vapor, but the reason for enhancement in latter is not clear yet. We detect moisture incursion from Arabian Sea, a phenomenon called atmospheric rivers (AR), land-falling intermittently along 12–25° N corridor of the west-coast of India during winter; using satellite and reanalysis data. The total vertically integrated horizontal water vapor transport in AR-landfalls ranging from 0.7 × 10⁸ to 2.2 × 10⁸ kg/s; nearly five-orders of magnitude larger than the average discharge of liquid water from Indus River into Arabian Sea. These AR events are playing prominent role in enhancing water vapor over IGP region by 19 ± 5%; in turn fueling the intensification of fog and haze through aerosol-water vapor interaction. We found that AR events enhanced aerosol optical depths over IGP by about 29 ± 13%. The progression of moist-laden winds in ARs onto Himalayan Mountains contributes to the precipitation that explains the observed rise in the extreme flow of western Himalayan Rivers in winter. We conclude that these ARs likely contribute to the decline of snow albedo as pollution-mixed-ARs encounter Hindukush-Karakoram-Himalayan mountain region.
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The Meiyu 2020 with record-breaking amount of precipitation, widespread area coverage and anomalous northern location brought about great social and economic impacts in China. However, the spatial property of anomalous rain-belt for such a catastrophic Meiyu is not well predicted. In this study, high-resolution in-situ observation and reanalysis data are used to explore key signals and possible prediction method. Results show that anomalous rain-belt of Meiyu (2020) is mainly influenced by the westward extended western North Pacific subtropical high (WNPSH) in the low-latitude and enhanced meridional circulation in mid-high latitudes. However, the distribution of composite anomalous circulation, especially in the mid-high latitude, cannot be revealed for 2020 if only considering the influence from the tropical Indo-Pacific thermal conditions. Through additional consideration of North Atlantic Oscillation (NAO), which has great contribution to circulation in the Northern Hemisphere mid-high latitudes, the anomalous key circulation features in 2020 can be appropriately captured. Also, the spatial property of anomalous rain-belt like 2020 could be accurately simulated by the established prediction model including combined effects of tropical Indo-Pacific thermal conditions and NAO. Specifically, quantified analyses prove that the warmed Indian Ocean plays a dominant role and anomalous NAO also has great importance for record-breaking area coverage and anomalous northern location of Meiyu (2020). Thus, for a more accurate prediction for anomalous rain-belt such as Meiyu 2020, the combined effects of both low- and mid-high-latitudes should be comprehensively considered.
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The Arctic temperature changes are closely linked to midlatitude weather variability and extreme events, which has attracted much attention in recent decades. Syntheses of proxy data from poleward of 60° N indicate that there was asymmetric cooling of -1.54 °C and -0.61 °C for Atlantic Arctic and Pacific Arctic during the Holocene, respectively. We also present a similar consistent cooling pattern from an accelerated transient Holocene climate simulation based on the Community Earth System Model. Our results indicate that the asymmetric Holocene Arctic cooling trend is dominated by the winter temperature variability with -0.67 °C cooling for Atlantic Arctic and 0.09 °C warming for Pacific Arctic, which is particularly pronounced at the proxy sites. Our findings indicate that sea ice in the North Atlantic expanded significantly during the Late Holocene, while a sea ice retreat is seen in the North Pacific, amplifying the cooling in the Atlantic Arctic by the sea ice feedback. The positive Arctic dipole pattern, which promotes warm southerly winds to the North Pacific, offsets parts of the cooling trend in Pacific Arctic. The Arctic dipole pattern also causes sea ice expansion in the North Atlantic, further amplifying the cooling asymmetry. We found that the temperature asymmetry is more pronounced in a simulation driven only by orbital forcing, indicating that the orbital modulation of the Pacific Decadal Oscillation, which in turn links to the Arctic dipole pattern, further affects the temperature asymmetry.
Thesis
Depuis l'ère préindustrielle, la température de surface en Arctique a augmenté plus de deux fois plus que la température globale : ce phénomène est appelé l'amplification arctique. Il a été montré que l’amplification arctique et le déclin de la glace de mer qui y est associé peuvent affecter la circulation atmosphérique de grande échelle, et ainsi impacter le climat des moyennes latitudes. Les mécanismes expliquant ce lien sont toutefois encore mal compris, et leur prépondérance par rapport aux autres composantes du système climatique demeure incertaine. L'objectif de cette thèse est de mieux comprendre ces mécanismes. Pour cela, nous avons isolé l'effet du déclin de la glace de mer arctique des autres forçages climatiques, à l'aide d'expériences de sensibilité réalisées avec le modèle de climat CNRM-CM6, à basse et haute résolution. Dans ces expériences, la valeur de l'albédo de la banquise est réduite à celle de l'océan, favorisant l'absorption de rayonnement solaire et la fonte de la glace, notamment en été. Nous avons dans un premier temps évalué l'état moyen du modèle et sa représentation des téléconnexions Arctique-moyennes latitudes. Cette évaluation suggère que l'augmentation de la résolution horizontale du modèle dans l'océan et dans l'atmosphère permet de simuler des conditions climatiques moyennes généralement plus réalistes. Nous avons montré par ailleurs que les téléconnexions liant la variabilité atmosphérique à celle de la glace de mer sont comparables entre le modèle et les observations. Les résultats indiquent que l'influence de la glace de mer arctique sur l'atmosphère est difficilement détectable dans les observations ou dans les simulations climatiques non contraintes à cause de la forte variabilité interne, ce qui justifie l'intérêt d'isoler cette influence et de réaliser des expériences de sensibilité telles que celles effectuées dans cette thèse. Nous nous sommes ensuite focalisés sur la réponse rapide de l'atmosphère durant l'automne et l'hiver qui suivent la disparition de la glace de mer d'été, c'est-à-dire lorsque l’amplification arctique est maximale. Les mécanismes de la réponse de la température à la fonte de la banquise ont été étudiés à l'échelle régionale grâce à une méthode d'ajustement dynamique basée sur la reconstruction régionale d'analogues de circulation. Les résultats montrent que le réchauffement en Amérique du Nord et en Europe induit par la perte de glace de mer arctique est principalement dû à : (i) des changements cycloniques de circulation qui favorisent des intrusions d'air chaud provenant du sud ou des océans adjacents, et (ii) des changements dits thermodynamiques -- sans changements de circulation. Ces derniers résultent à la fois de l'advection d'air chaud par le flux moyen, provenant de l'Arctique et/ou des océans adjacents réchauffés en réponse au déclin de la glace de mer, et à la fois des modifications locales du budget énergétique de surface. La diminution de la glace de mer dans ces expériences favorise également un refroidissement en Asie centrale, qui est ici entièrement expliqué par des changements de circulation, associés à un renforcement de l'anticyclone de Sibérie. La réponse atmosphérique de grande échelle a par ailleurs été étudiée dans la troposphère et la stratosphère. Les résultats indiquent que la stratosphère joue un rôle minimal dans l'évolution de la circulation dans la troposphère et à la surface dans ces expériences. Enfin, nous avons montré que ni l'augmentation de la résolution, ni la modification des conditions de forçages externes entre des conditions préindustrielles et des conditions de milieu du XXème siècle n'impacte de manière significative la réponse de l'atmosphère de grande échelle au déclin de la banquise arctique dans le modèle CNRM-CM6. Les analyses effectuées dans cette thèse mettent en évidence la difficulté de détecter une réponse robuste de l'atmosphère en saison froide du fait de la forte variabilité interne et de la faible réponse.
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Successive cold winters of severely low temperatures in recent years have had critical social and economic impacts on the mid-latitude continents in the Northern Hemisphere. Although these cold winters are thought to be partly driven by dramatic losses of Arctic sea-ice, the mechanism that links sea-ice loss to cold winters remains a subject of debate. Here, by conducting observational analyses and model experiments, we show how Arctic sea-ice loss and cold winters in extra-polar regions are dynamically connected through the polar stratosphere. We find that decreased sea-ice cover during early winter months (November-December), especially over the Barents-Kara seas, enhances the upward propagation of planetary-scale waves with wavenumbers of 1 and 2, subsequently weakening the stratospheric polar vortex in mid-winter (January-February). The weakened polar vortex preferentially induces a negative phase of Arctic Oscillation at the surface, resulting in low temperatures in mid-latitudes.
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There has been an ostensibly large number of extreme weather events in the Northern Hemisphere mid-latitudes during the past decade(1). An open question that is critically important for scientists and policy makers is whether any such increase in weather extremes is natural or anthropogenic in origin(2-13). One mechanism proposed to explain the increased frequency of extreme weather events is the amplification of mid-latitude atmospheric planetary waves(14-17). Disproportionately large warming in the northern polar regions compared with mid-latitudes-and associated weakening of the north-south temperature gradient-may favour larger amplitude planetary waves(14-17), although observational evidence for this remains inconclusive(18-21). A better understanding of the role of planetary waves in causing mid-latitude weather extremes is essential for assessing the potential environmental and socioeconomic impacts of future planetary wave changes. Here we show that months of extreme weather over mid-latitudes are commonly accompanied by significantly amplified quasi-stationary mid-tropospheric planetary waves. Conversely, months of near-average weather over mid-latitudes are often accompanied by significantly attenuated waves. Depending on geographical region, certain types of extreme weather (for example, hot, cold, wet, dry) are more strongly related to wave amplitude changes than others. The findings suggest that amplification of quasi-stationary waves preferentially increases the probabilities of heat waves in western North America and central Asia, cold outbreaks in eastern North America, droughts in central North America, Europe and central Asia, and wet spells in western Asia.
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This study uses cluster analysis to investigate the interdecadal poleward shift of the subtropical and eddy-driven jets and its relationship to intraseasonal teleconnections. For this purpose, self-organizing map (SOM) analysis is applied to the ECMWF Interim Re-Analysis (ERA-Interim) zonal-mean zonal wind. The resulting SOM patterns have time scales of 4.8–5.7 days and undergo notable interdecadal trends in their frequency of occurrence. The sum of these trends closely resembles the observed interdecadal trend of the subtropical and eddy-driven jets, indicating that much of the interdecadal climate forcing is manifested through changes in the frequency of intraseasonal teleconnection patterns. Two classes of jet cluster patterns are identified. The first class of SOM pattern is preceded by anomalies in convection over the warm pool followed by changes in the poleward wave activity flux. The second class of patterns is preceded by sea ice and stratospheric polar vortex anomalies; when the Arctic sea ice area is reduced, the subsequent planetary wave anomalies destructively interfere with the climatological stationary waves. This is followed by a decrease in the vertical wave activity flux and a strengthening of the stratospheric polar vortex. An increase in sea ice area leads to the opposite chain of events. Analysis suggests that the positive trend in the Arctic Oscillation (AO) up until the early 1990s might be attributed to increased warm pool tropical convection, while the subsequent reversal in its trend may be due to the influence of tropical convection being overshadowed by the accelerated loss of Arctic sea ice.
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Over the past decade, severe winters occurred frequently in mid-latitude Eurasia, despite increasing global- and annual-mean surface air temperatures. Observations suggest that these cold Eurasian winters could have been instigated by Arctic sea-ice decline, through excitation of circulation anomalies similar to the Arctic Oscillation. In climate simulations, however, a robust atmospheric response to sea-ice decline has not been found, perhaps owing to energetic internal fluctuations in the atmospheric circulation. Here we use a 100-member ensemble of simulations with an atmospheric general circulation model driven by observation-based sea-ice concentration anomalies to show that as a result of sea-ice reduction in the Barents–Kara Sea, the probability of severe winters has more than doubled in central Eurasia. In our simulations, the atmospheric response to sea-ice decline is approximately independent of the Arctic Oscillation. Both reanalysis data and our simulations suggest that sea-ice decline leads to more frequent Eurasian blocking situations, which in turn favour cold-air advection to Eurasia and hence severe winters. Based on a further analysis of simulations from 22 climate models we conclude that the sea-ice-driven cold winters are unlikely to dominate in a warming future climate, although uncertainty remains, due in part to an insufficient ensemble size.
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Atmospheric fronts are important for the day-to-day variability of weather in the midlatitudes. It is therefore vital to know how their distribution and frequency will change in a projected warmer climate. Here we apply an objective front identification method, based on a thermal front parameter, to 6-hourly data from models participating in CMIP5. The historical simulations are evaluated against ERA-Interim and found to produce a similar frequency of fronts and with similar front strength. The models show some biases in the location of the front frequency maxima. Future changes are estimated using the high emissions scenario simulations (RCP8.5). Projections show an overall decrease in front frequency in the Northern Hemisphere, with a poleward shift of the maxima of front frequency and a strong decrease at high latitudes where the temperature gradient is decreased. The Southern Hemisphere shows a poleward shift of the frequency maximum, consistent with previous storm-track studies.