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Laser-induced water condensation in air
Philipp Rohwetter1,Je
´ro
ˆme Kasparian2*, Kamil Stelmaszczyk1, Zuoqiang Hao3, Stefano Henin2,
Noe
¨lle Lascoux3, Walter M. Nakaema1,YannickPetit
2, Manuel Queißer1, Rami Salame
´3,
Estelle Salmon3, Ludger Wo
¨ste1and Jean-Pierre Wolf2
Triggering rain on demand is an old dream of mankind, with a huge potential socio-economical benefit. To date, efforts
have mainly focused on cloud-seeding using silver salt particles. We demonstrate that self-guided ionized filaments
generated by ultrashort laser pulses are also able to induce water-cloud condensation in the free, sub-saturated
atmosphere. Potential contributing mechanisms include photo-oxidative chemistry and electrostatic effects. As well as
revealing the potential for influencing or triggering water precipitation, laser-induced water condensation provides a new
tool for the remote sensing of nucleation processes in clouds.
Global warming and stratospheric ozone depletion have
demonstrated that human activities can significantly alter
the climate of Earth. However, the potential to locally alter
or even control the weather is still the subject of intensive
debate1,2. There have been long-standing efforts dedicated to
seeding clouds3with silver salt particles to encourage precipitation.
Here, we demonstrate that self-guided ionized filaments4–8 gener-
ated by ultrashort laser pulses are also able to induce water cloud
condensation in the free, sub-saturated atmosphere. In additional
laboratory experiments under both saturated and sub-saturated con-
ditions, we estimate a water uptake rate of up to 5 mg cm
23
s
21
in
the active volume of the filament-induced plasma channels. We
briefly discuss possible mechanisms that could contribute to this
observed laser-induced water condensation, although further inves-
tigations are needed to fully clarify their roles. Laser-based conden-
sation provides a new tool for the remote sensing of nucleation
processes in clouds and may even open up the possibility of influen-
cing or triggering water precipitation.
Self-guided laser filaments result from a nonlinear propagation
regime of ultra-short laser pulses. Beyond a critical power (P
cr
¼
3 GW in air at a wavelength of 800 nm), the beam self-focuses due
to the optical Kerr effect until its intensity is sufficient to allow
multiphoton ionization of air molecules, generating a cold plasma.
At this point, the released free electrons (typically 10
15
–10
16
cm
23
)
and the negative higher-order Kerr terms9tend to defocus the
beam and dynamically balance Kerr self-focusing. As a result, one
or several self-guided filaments10 with a diameter of 100 mmare
generated over distances much longer than the Rayleigh length,
up to hundreds of metres11. Filaments can be initiated at predefined
remote distances12 and propagate through adverse conditions
including fog and clouds10, turbulence13,14 or reduced pressures15.
They are therefore well suited for atmospheric applications4,7,even
in perturbed atmospheres.
We recently demonstrated that laser filaments can trigger corona
discharges within thunderclouds16, opening the way to lightning
control applications. With the present demonstration of water conden-
sation, self-guided filaments also raise new hopes that laser-assisted
local weather modification may be achieved, which, in contrast to
cloud-seeding using rockets, could be operated continuously and
would be free of environmental side effects.
Experiments
As detailed in the Methods, experiments were conducted both in the
free atmosphere and under controlled conditions in a diffusion
cloud chamber filled with ambient air. A bundle of 20 to 30 self-
guided filaments was generated by the Teramobile femtosecond-
terawatt laser17, which provided 220-mJ pulses with a duration of
60 fs (3.5 TW peak power) at a central wavelength of 800 nm and
a repetition rate of 10 Hz. The filamentation onset was adjusted
by providing a negative chirp to the emitted laser pulse, so that
the group velocity dispersion (GVD) in the air recompressed the
pulse at a distance chosen for the interaction with the air mass
under investigation, either in the atmospheric cloud chamber or
in the free atmosphere.
Results and discussion
Highly reproducible filament-induced water condensation trails
were observed with the naked eye (see Fig. 1a,b and
Supplementary Movie) when the filaments were launched into the
atmospheric cloud chamber at a saturation of S¼2.3+0.7 (that
is, a relative humidity, RH¼230+70%) and a temperature
T¼224 8C. In ten experiments, we were able to confirm this quali-
tative observation by recording the corresponding evolution of
droplet density and size distribution using a Malvern Spraytec
aerosol particle sizer (see typical result in Fig. 1c,d). The particle
sizer gave access to particles greater than 2.4 mm only, so the con-
densation nuclei (CN) and cloud condensation nuclei (CCN)
could not be detected. The initial size distribution featured three
modes at diameters of 4, 50 and 250 mm. The droplet density in
each size class fluctuated significantly due to the residual air turbu-
lence in the chamber and the corresponding inhomogeneous distri-
bution of the pre-existing aerosols. However, a Student t-test
comparing the measured signals before and after the laser shot
confirmed that the observed effect has a statistical significance of
12
a
.0.9995. After the laser was fired, the average diameter of
the small particles grew to 6 mm, and their density dropped by
half, a change well beyond the fluctuations recorded before the
laser pulse. The total water content of this smaller mode therefore
remained almost constant. The decrease of this mode is most prob-
ably due to the coalescence of droplets, particularly the bigger ones.
This coalescence process is sustained by the mutual attraction of
1Teramobile, Institut fu¨r Experimentalphysik, Freie Universita
¨t Berlin, Arnimallee 14, D-14195 Berlin, Germany, 2Teramobile, GAP, Universite
´de Gene
`ve,
20 rue de l’Ecole de Me
´decine, CH-1211 Gene
`ve 4, Switzerland, 3Teramobile, Universite
´Lyon 1; CNRS; LASIM UMR 5579, ba
ˆtiment A. Kastler, 43 Boulevard
du 11 novembre 1918, F-69622 Villeurbanne Cedex, France. *e-mail: jerome.kasparian@unige.ch
ARTICLES
PUBLISHED ONLINE: 2 MAY 2010 | DOI: 10.1038/NPHOTON.2010.115
NATURE PHOTONICS | ADVANCE ONLINE PUBLICATION | www.nature.com/naturephotonics 1
© 2010 Macmillan Publishers Limited. All rights reserved.
particles bearing opposite net charges generated in amounts of
10
15
–10
16
charges cm
23
by the filaments18.
Simultaneously, the density of the mode around 50 mm doubled.
Figure 1c clearly shows that this mode does not develop from
smaller droplets, because these two modes remain distinct through-
out the growth sequence. Rather, the sudden rise in the medium
mode shortly after the laser fired probably stems from the laser-
induced fragmentation of droplets from the larger mode at
250 mm. The 50-mm droplets then grew to 80 mm within 3 s.
Simultaneously, the biggest mode also grew towards 400 mm. As a
consequence of this growth, the total atmospheric content of con-
densed water, as determined by integrating the volume of the dro-
plets over the measured size distribution and averaging over the
beam, increased by half (þ70 mgcm
23
). Considering that the
100-mm filaments only occupy 0.5% of the laser beam volume,
the local increase within the filament active volume amounted to a
factor of 100 (15 mg cm
23
), that is, 5 mg cm
23
s
21
over the 3 s of
growth time. Such results provide clear evidence of filament-assisted
condensation. The final droplet diameter of 80 mm was twice as big
as that predicted by a diffusive growth model for pure water under
thermodynamically stable conditions19 (that is, growth limited by
the local depletion of water vapour). Their growth rate of
10 mms
21
was four times faster, probably due to Wilson-type20
enhancement of the growth rate of the droplets charged by their
exposure to the high-charge density generated by the filaments.
However, the Wilson mechanism is not the only mechanism
that can explain laser-induced water vapour condensation,
because a dramatic and highly reproducible effect was also observed
in sub-saturated conditions (Fig. 2). We varied the relative humidity
in the chamber between 70 and 90% and the temperature between
20 and 60 8C. The observation of an increase in probe light scatter-
ing was governed by thewater content of the atmosphere rather than
by the relative humidity. Condensation was observed only when this
was above 80 mgcm
23
provided the relative humidity exceeded
75%. In such conditions, a 30-s series of 300 multifilamenting
laser pulses resulted in an immediate rise in the scattering signal
by a factor of 10, followed by a slower increase up to a factor of
25 with a time constant
t
≈4 s (Fig. 2). Such a steep rise again pro-
vides clear evidence of an increase in droplet size and number
density in the chamber, consistent with observations with the naked
eye. Moreover, saturation of the growth rate is typical of a process
limited by vapour depletion and the diffusion rate of vapour into
the beam region. In contrast, lower water vapour concentrations
did not allow substantial condensation even at RH ¼95%. The
requirement for condensable water before a visible effect is seen
shows that it is water vapour condensation indeed that is observed.
This condensation is not affected by the heat deposited by the
laser filaments into the air. A typical filament5–8 with an intensity
of 50 GW cm
22
, diameter of 100 mm and pulse duration of 100 fs
carries 0.4 mJ of energy. Even if this energy was totally absorbed
over a 10-m length of air, the specific heat of 1 kJ kg
21
K
21
and
the density of 1.2 kg m
23
would yield a temperature increase
limited to 3.3 K. In fact, only a small fraction of the filament
energy is absorbed, so heating of the air can be neglected in the
analysis of our results, and the ambient temperature can be con-
sidered as representative of the conditions within the filaments.
0
−1
−2
Time relative to laser pulse (s)
1
2
3
4
5
2.4 7.2 18 101 240 48042
Diameter (µm)
Droplet density (cm
3
/size class)
100
1
10−2
10−3
103
10
0.1
10−4
Total condensed mass (µg cm−3)
c
a
d
b
1,600
5 mm
0
800
1,200
5−2 −1 0 1 2 3 4
400
100
150
200
250
Time relative to laser pulse (s)
Total condensed mass
Small droplets (<20µm)
Medium droplets
(20−100µm) (×50)
Droplet density (cm−3)
5 mm
Figure 1 |Laser-induced condensation in an atmospheric cloud chamber (T5224 88888CandRH5230%). a,b, View inside the chamber before (a)andafter
(b) firing a set of three laser shots at 100-ms intervals. The laser filaments induce macroscopically visible droplet condensation, as is evident from the
massive increase in light scattering (see also the Supplementary Movie). c,d, Effect of a pair of laser shots launched in the chamber at t¼0andt¼0.1 s.
Temporal evolution of the particle size distribution (c) and the amount of small and medium droplets (d, left axis) as well as the total condensed water mass
(d, right axis) per unit volume. The arrows indicate the correspondence between the modes of the size distribution on panel c, and the curves displaying
their mode-integrated droplet density on panel d.
ARTICLES NATURE PHOTONICS DOI: 10.1038/NPHOTON.2010.115
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© 2010 Macmillan Publishers Limited. All rights reserved.
This negligible heating of the air contrasts with the high electron
temperature in the plasma filament, which can reach up to
6,000 K (refs 5–8). It should be noted that, due to the small trans-
verse dimension of the filaments, the slight local heating of the air
results in large temperature gradients, leading to the development
of a shockwave21. The corresponding expansion of the air might
contribute to the condensation process.
Note also that the fragmentation of pre-existing water droplets
into smaller ones increases the scattering signal. We quantified
this effect by modelling the laser-induced droplet fragmentation,
considering that each mother droplet absorbs an amount of
energy proportional to its cross-section, part of which is turned
into additional surface energy during fragmentation. A one-step
fragmentation model based on a maximum entropy principle
results in a Poissonian size distribution of the fragments of each
mother droplet22. By treating this distribution as continuous, even
in cases where it contained only a few tens of daughter particles23,
we found that the contribution of laser-induced droplet fragmenta-
tion to the effect observed in the sub-saturated cloud chamber was
marginal, regardless of whether nonlinear absorption or linear
absorption were considered. Instead, the observed condensation
may be understood by remembering that the atmospheric cloud
chamber is filled with ambient air. Therefore, in the urban
environment of the laboratory (including aerosols and gaseous
pollutants) and in the presence of the high-intensity laser
field, photochemically or charge-assisted mechanisms contribute
significantly to droplet formation24–26.
To provide a definitive demonstration of the capability of laser
filaments to trigger condensation, not only in controlled laboratory
conditions but also in real atmospheric conditions, we performed
open-field experiments (Fig. 3a) in the late autumn of 2008 in
Berlin, Germany, under conditions of polar air mass, providing a
high relative humidity (RH ¼90–93%) together with low level of
background aerosols (70 km horizontal visibility). The laser was
launched vertically into the atmosphere, at a repetition rate of
5 Hz. The filaments were most active between heights of 45 and
75 m. Their strength then decreased over a few tens of metres
beyond this range. The aerosol content of the atmosphere was mon-
itored by LIDAR (light detection and ranging)27 using a low-power
frequency-doubled Nd:YAG laser at 10 Hz repetition rate. This
allowed the performance of differential measurements of the
changes induced by the terawatt laser pulses preceding the LIDAR
pulses (Fig. 3a). The LIDAR return signals provide range-resolved
measurements of the total volume backscattering coefficient
b
,
which comprises a molecular contribution (Rayleigh scattering is
subtracted in the data processing) and an aerosol contribution
(Mie scattering). This aerosol backscattering coefficient
b
Mie
is
defined as27
b
Mie =1
0
Nr()
d
s
n,r()
dV
u
=p
dr(1)
where N(r) is the number density of droplets of size r, and
d
s
n,r()/dV
u
=pis the size- and refractive index-dependent back-
scattering differential cross-section of the particles.
b
Mie
therefore pro-
vides information averaged over all aerosol types and sizes within
the probed volume.
The LIDAR measurements were taken 1 ms after firing the tera-
watt laser pulses. This time delay, much shorter than typical droplet
growth times, was imposed by a lateral wind sweeping the air
ionized by the filaments out of the detection volume. As already
mentioned above, the filaments occupy a fraction of only 2.5 ×10
24
of the air volume probed by the LIDAR. Despite those difficulties
and atmospheric fluctuations, the beam-averaged value of
b
Mie
at
the height of the filaments was up to 0.5% higher when following a
filamenting laser pulse than without filaments (Fig. 3b). This
increase corresponds to a local enhancement of Mie scattering by a
factor of 20 within the filaments, from
b
Mie
¼1×10
26
m
21
sr
21
to
2×10
25
m
21
sr
21
. The latter value is typical of haze27,inspiteofa
growth time of 1 ms, much shorter than the signal rise time identified
in the sub-saturated chamber (Fig. 2b). Because
b
Mie
is a measure of all
kinds of aerosols, one could argue that only sulphate and nitrate CN or
CCN were observed. However, the results of the experiment in the
sub-saturated chamber discussed above show that the laser filaments
also cause the subsequent condensation of water droplets provided
enough water vapour is available in the atmosphere.
The statistical significance of the observed effect was assessed by
a Mann–Whitney U-test, comparing the sets of LIDAR signals fol-
lowing a filamenting pulse with the reference LIDAR signals. The
null-hypothesis of this non-parametric test is that the two samples
are drawn from a single population, so their probability distri-
butions are equal. It therefore makes no assumption about the
shape of the underlying distribution(s) and is insensitive to outliers.
The Mann–Whitney test can be seen as assessing for differences in
medians of the considered distributions. Statistically significant
results (
a
,0.01, where 1 2
a
is the confidence level) were obtained
between 6:00 and 6:30, when temperature and relative humidity
were 2.9 8C and 90%, respectively.
Afterwards, the meteorological conditions changed. A reduction
in the visibility, a slow increase in the relative humidity up to 93%
over 2 h and a rise in the absolute value of the LIDAR signal
suggested an increase in the background concentration of water
aerosols. Correlatively, the effect of filament-induced condensation
on the backscattering signal faded into the background. The fact
b
a
1,0005000
0.0
0.2
0.4
0.6
0.8
1.0
Normalized counts
0 5 10 15 20 25 30
0.0
0.1
0.2
0.3
0.4
0.5
1 50 100 150 200 250 300
Time after first shot (s)
Laser shot no.
Mean normalized counts
Time (s)
Laser ON time
Scattering signal
Background
Exponential fit, τ=4s
Figure 2 |Laser-induced condensation in a sub-saturated atmospheric
cloud chamber (T560 88888C, RH 575–85%), observed through the
scattered signal at 9088888.a, High reproducibility of the effect over repeated
laser on/off cycles of 300 laser shots each. b, Rise time (time constant
t
≈4 s) of the light scattered by the growing droplets, averaged over the 17
cycles of panel a.
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© 2010 Macmillan Publishers Limited. All rights reserved.
that the observed effects depend on the weather conditions excludes
a systematic experimental flaw. Furthermore, we can exclude direct
contribution of the filament plasma to the LIDAR signal, because
the lifetime of the plasma generated by the filaments does not
exceed the microsecond timescale, well below the millisecond
interval between the pump and the probe pulses28.
As in the cloud chamber experiment, we checked that the
enhancement of the LIDAR signal by the laser filaments could
not be explained by laser-induced aerosol fragmentation. First, the
observed effect decreases when the background LIDAR signal
increases, that is, when more water droplets are available for frag-
mentation. The above-described model of droplet fragmentation
quantitatively confirmed this qualitative argument. Based on very
high-visibility conditions and air-mass back trajectories29, we con-
sidered an initial maritime haze size distribution30. The visibility
provided the water droplet concentration, which was equal to
136 mm
23
. Alternative rural, remote continental and urban size
distributions were also considered, without affecting the result
qualitatively. Between 8 and 400 fragments per mother droplet
were considered, with refractive indices in the range 1.3–1.5 com-
monly encountered in hazes31. Even if an overestimation of the fila-
ment number (100) and diameter (200 mm) were taken into account
in the calculations, we found that fragmentation could increase the
Mie backscattering coefficient by at most 0.1–0.2%. Thus, fragmen-
tation does not provide the dominant contribution to the observed
effect in the atmospheric experiments.
Systematic parametric measurements would be required to better
understand and optimize the complex processes at play in our
observations. Although such a study is beyond the scope of the
present work, some important facts have to be considered. Each fila-
ment generates a cold plasma5–8 with 10
15
–10
16
electrons cm
23
(ref. 5), that is, an average charge generation rate of 10
11
charges cm
23
s
21
at a repetition rate of 10 Hz. Most of these elec-
trons attach to ions within a few picoseconds while, typically,
ab
0.0 0.2 0.4 0.6
0
20
40
60
80
100
120
140
Relative increase of
Mie backscattering (%)
Height (m)
Teramobile:
800 nm, 220 mJ,
120 fs, 5 Hz
LIDAR transmitter:
532 nm, 5 mJ, 7 ns, 10 Hz
PC
Ref. PD
Telescope
Backscattered
light Filamenting
Teramobile
beam
Fibre bundle
Digital
oscilloscope
Filter +
photomultiplier
1 ms
Figure 3 |Laser-induced condensation experiment in the atmosphere. a, Experimental set-up. The Teramobile laser (red) is fired 1 ms before the LIDAR
pulse (green) measuring the aerosol content of the atmosphere. b, Time-averaged relative increase of the Mie backscattering coefficient
b
Mie
measured
between 6:00 and 6:30 with and without firing the Teramobile laser. The signal enhancement at the height of the filaments (the most active filamenting
region at 45–75 m is shaded) is a clear indication for filament-induced condensation.
A
B
D
C
E
F
ab
051015
0
1
2
3
4
5
6
220
230
240
250
260
270
280
290
Height in chamber (cm)
Laser position
Saturation ratio
T (K)
Figure 4 |Atmospheric diffusion chamber for laboratory experiments. a, Experimental set-up (schematic). A, Teramobile beam; B, particle sizer laser beam;
C, particle sizer receiver unit; D, imaging charge-coupled device camera; E, heat and vapour source; F, cold bottom plate. b, Measured vertical temperat ure
(blue, right scale) and derived supersaturation profile (red, left scale) in the chamber. The dashed lines correspond to the worst-case combinations of 2
s
temperature and chamber top saturation measurement errors. The grey region indicates the position of the laser beam.
ARTICLES NATURE PHOTONICS DOI: 10.1038/NPHOTON.2010.115
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© 2010 Macmillan Publishers Limited. All rights reserved.
10
13
cm
23
of them attach to O
2
molecules to form O
2
2
ions, which
last for several microseconds5. These oxygen ions can form Wilson
clusters24 with high efficiency due to the extremely high initial con-
centration of O
2
2
, even without photoactivation. Direct multipho-
ton water photolysis25 can further contribute to this process
because the intensity of 50 GW cm
22
in the filaments allows pro-
cesses that are usually only considered for UV lasers. However, ther-
mally driven chemical reactions are not to be considered, because, as
discussed above, the plasma generated by the filaments is cold5–8.
The exceptionally high charge density could also result in a pro-
duction rate of oxidizing molecules such as O
3
and
†
OH radicals
that is orders of magnitude above the natural rates found in the
atmosphere. The resulting
†
OH, together with the O
2
2
ions men-
tioned above, will rapidly produce Wilson clusters25, oxidize SO
2
(refs 26,32) and NO
2
into H
2
SO
4
and HNO
3
, respectively, and
assist their heterogeneous nucleation as well as that of volatile
organic species. Such processes are indeed compatible with the
millisecond timescale of the observed process. Most of these aero-
sols are highly hygroscopic and will later serve as CCN, allowing
the growth of water droplets in adequate humidity conditions, as
demonstrated in the sub-saturated cloud chamber experiment.
However, at the time of the probe pulse, the scattering efficiencies
are still low because the droplets have not had time to grow.
Conclusions
As a conclusion, we have experimentally demonstrated that self-
guided filaments generated by ultrashort laser pulses can assist
water condensation, even in an undersaturated free atmosphere.
Potential contributing mechanisms include photo-oxidative chem-
istry and electrostatic effects. The phenomenon provides a new
and attractive tool for remote characterization of the humid atmos-
phere and cloud formation. In addition, it may even provide the
potential to influence or trigger water precipitation using continu-
ously operating lasers rather than rockets.
Methods
The Teramobile femtosecond–terawatt laser17 used to generate the filaments
provided 220-mJ pulses of 60-fs duration at 800 nm, with a repetition rate of 10 Hz.
The beam formed a bundle of 20–30 filaments. In laboratory experiments, it was
launched through a diffusion chamber33 (Fig. 4a) filled with ambient air, as single
shots or in bursts of up to 30 s in duration. The filaments typically started a few
metres before the chamber, which was positioned 15 m away from the laser output.
A strong temperature gradient was maintained in the chamber volume of
0.6 ×0.3 ×0.2 m3by using a cold base plate that was kept at 260 8C by indirect
contact with a liquid-nitrogen reservoir, and a thermostated circulator heated to
10 8C at the top of the chamber. Water vapour from a reservoir at the top of the
chamber diffused towards the bottom plate. We estimated the relative humidity at
the top of the chamber to be 42+10% by measuring the evaporation time of
51+1 min of sessile water drops with an initial volume of 2 ml (ref. 34). The typical
vertical temperature profile, measured with a K-type thermocouple, is shown in
Fig. 1b. This profile was used to estimate the supersaturation profile, assuming steady
state35 and a zero water vapour concentration at the bottom of the chamber. The
supersaturation was estimated to be S≈4 near the bottom of the chamber,
consistent with the fact that we operated the chamber slightly below the threshold of
sensitivity to cosmic rays36. The resulting supersaturation in the interaction region
was S¼2.3+0.7 at a temperature of T≈224 8C. Sub-saturated conditions were
obtained by installing a water reservoir that was maintained above 100 8C at the top
of the cloud chamber while its bottom was circulator cooled to þ11 8C. The relative
humidity at the position of the beam was monitored with a capacitance hygrometer.
It ranged between 75 and 85% (S¼0.75–0.85) at a local temperature of 60 8C.
The water aerosol density in the atmospheric cloud chamber was observed with
the naked eye and monitored by launching a low-powercontinuous wave (c.w.) laser
(Nd:YAG, 532 nm, 10 mW) across the path of the pump beam and observing the
scattering at 908or 458. Scattering is a signature of water droplets, because Rayleigh
scattering by air molecules within the cell is negligible at atmospheric pressure over
the considered metre scale. Alternatively, the particle size distribution was
monitored by measuring the angular distribution of the scattered light of a He:Ne
laser in the forward direction using a Malvern Spraytec particle sizer. The data were
inverted using Mie theory, while considering the dominant particles to be spherical
water droplets.
The atmospheric experiment was performed at night in late autumn of 2008 in
Berlin (52827′24′′ N, 13817′38′′ E, 55 m above sea level), under conditions of
incoming arctic cold air (2.9 8C) and initially strong westerly winds at an
atmospheric pressure of 995 hPa, with a relative humidity initially stable at 90%
over 1 h and then slowly rising to 93% over 2 h. The horizontal visibility and wind
speed and direction were measured 33 and 39 m above ground, respectively, 1,140 m
east of the experimental location. Temperature and relative humidity were recorded
upwind at 620 m in the east–south–east direction away from the experimental site.
The initial horizontal standard visibility was 70 km, indicating an exceptionally
low background of aerosol scatterers. This value was used to calibrate the
aerosol-related fraction of the atmospheric backscattering coefficient from the
LIDAR signals.
In this experiment (Fig. 3), the Teramobile beam was expanded to a diameter of
10 cm and launched vertically into the free atmosphere at a repetition rate of 5 Hz.
The pulses were chirped and the beam slightly focused to maximize the strength of
multiple filamentation at a distance of 60 m. Backscattering from the atmosphere
was probed with a LIDAR using a 5-mJ YAG laser beam at 532 nm, pulsed at 10 Hz,
emitted collimated with a beam diameter of 4 cm, and overlapped with the
Teramobile beam on a dichroic mirror. This overlap was checked at 0 and 60 m by
folding the beams horizontally, ensuring that the strongly filamenting region was
effectively superposed with the probe beam.
The probe beam alternately measured the backscattering 1 ms following a
Teramobile shot and then in unaffected atmosphere 100 ms following the shot. The
horizontal wind speed of 2.5–5 m s
21
ensured that each pulse (resp. pulse pair)
interacted with a fresh air column. Single-shot LIDAR transients were collected with
a 11.4-cm-diameter, f¼500 mm telescope (4 mrad field of view), 20 cm off the axis
of the laser beam, detected by a photomultiplier tube equipped with a narrowband
(1 nm bandwidth full-width at half-maximum (FWHM) at 532 nm) interference
filter, and recorded on a digital oscilloscope used as a transient recorder (500 MHz
bandwidth). Each individual LIDAR signal was normalized by the pulse energy of
the probe pulses, as recorded using a high-speed photodiode. The inclination
between the axes of the laser beams and of the telescope provided 100% overlap
around 60 m, in the filamenting region. We integrated the LIDAR signals generated
by probe pulses over the most active filamenting region, between altitudes of 45 and
75 m (shaded region of Fig. 3), and compared those following a Teramobile pulse
with reference pulses.
Received 11 November 2009; accepted 8 March 2010;
published online 2 May 2010
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Acknowledgements
The authors would like to acknowledge J. Kirkby of CERN for fruitful discussions,
I. Sorge of Institut fu
¨r Meteorologie, FU-Berlin, Germany, for providing weather data,
and T. L. Kucsera (GEST) at NASA/Goddard for back-trajectories (available at the
aeronet.gsfc.nasa.gov website). This work was supported by the Deutsche
Forschungsgemeinschaft, Agence Nationale de la Recherche (ProjectANR-05-Blan-0187),
the Fonds National Suisse de la Recherche Scientifique (FNS, grant nos. 200021-116198 and
200021-125315), and the Swiss Secre
´tariat d’E
´tat a
`l’E
´ducation et a
`la Recherche in the
framework of the COST P18 project ‘The Physics of Lightning Flash and its Effects’.
Author contributions
All authors contributed extensively to the work presented in this paper. More specifically,
P.R., J.K., K.S., L.W. and J.-P.W. conceived and designed the study. P.R., K.S., Z.H., S.H.,
N.L., W.N., Y.P., M.Q., R.S. and E.S. perf ormed the experiments.P.R., J.K. and K.S. analysed
the data, and J.K., L.W. and J.-P.W. wrote the paper.
Additional information
The authors declare no competing financial interests. Supplementary information
accompanies this paper at www.nature.com/naturephotonics.
Reprints and permission
information is available online at http://npg.nature.com/reprintsandpermissions/.
Correspondence and requests for materials should be addressed to J.K.
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