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JOURNAL OF GEOPHYSICAL RESEARCH, VOL. 113, D12113, doi:10.1029/2007JD009313, 2008

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ArticleIsotope ratios of precipitation and water vapor observed in
Typhoon Shanshan
H. Fudeyasu,1 K. Ichiyanagi,1 A. Sugimoto,2 K. Yoshimura,3 A. Ueta,2 M. D. Yamanaka,1and K. Ozawa4
Received 23 August 2007; revised 22 January 2008; accepted 14 February 2008; published 26 June 2008.

[1] Isotope ratios of precipitation and water vapor were observed during the passage ofTyphoon Shanshan at Ishigaki Island, southwestern Japan, on 15–16 September 2006.
Such high-resolution isotopic observations allow for qualitative understanding of
atmospheric moisture cycling; they revealed that isotope ratios of both the precipitation
and water vapor decreased radially inward in the cyclone’s outer region; anomalously
high isotope ratios appeared in the cyclone’s inner region; and d-excess tended to decreasein the cyclone’s inner region. In the cyclone’s outer region, the water vapor was
isotopically depleted due to the rainout effect which involves both condensation efficiency
as reflected in inwardly increasing cloud thickness and isotopic exchange between
falling droplets and the ambient water vapor. In contrast, water vapor in the cyclone’s
inner region was isotopically enriched due to weak rainout effect in conjunction withintensive isotopic recharge from the sea spray and sea surface with heavy isotope ratios.
Since water vapor mainly acts as a source of precipitation, the isotope ratios ofprecipitation also had systematic variation. A unique circumstance is the intensity of
isotopic exchange with almost saturated surface air and high winds, causing anomalously
high isotope ratios and low d-excess values in the cyclone’s inner region.
Citation: Fudeyasu, H., K. Ichiyanagi, A. Sugimoto, K. Yoshimura, A. Ueta, M. D. Yamanaka, and K. Ozawa (2008), Isotope ratiosof precipitation and water vapor observed in Typhoon Shanshan, J. Geophys. Res., 113, D12113, doi:10.1029/2007JD009313.

1. Introduction[2] A number of studies have examined intensification oftropical cyclones (TCs) over the ocean [e.g., Ooyama, 1964,
1969; Charney and Eliassen, 1964; Rotunno and Emanuel,1987; Emanuel, 1989; Montgomery et al., 2006]. The mainenergy source of a TC is the water derived from evaporationfrom a tropical ocean and/or converging water vapor in theatmospheric boundary layer from environmental moisturesurrounding the TC. While atmospheric moisture cycling
plays a central role in TC intensification, few observationsof such moisture cycling are available. Stable hydrogenand oxygen isotope ratios (2H1H16O/1H2 16O and 1H2 18O/
1
H2 16O) are dynamic tracers of atmospheric moisture cycling
because their compositions are physically influenced bycomplex atmospheric behavior, water vapor advection,condensation, and evaporation. Many observational studies
have examined isotopes of precipitation and water vapor[e.g., Ichiyanagi et al., 2005].
1
Japan Agency for Marine-Earth Science and Technology, Institute ofObservational Research for Global Change, Yokosuka, Kanagawa, Japan.
2
Hokkaido University, Graduate School of Environmental Science,
Sapporo, Hokkaido, Japan.
3
University of Tokyo, Institute of Industrial Science, Tokyo, Tokyo,
Japan.
4
Japan International Research Center for Agricultural Sciences, Tropical
Agriculture Research Front, Ishigaki, Okinawa, Japan.

Copyright 2008 by the American Geophysical Union.
0148-0227/08/2007JD009313$09.00[3] Lawrence and Gedzelman [1996] suggested the use of
stable isotope ratios to investigate the moisture cycling ofTCs. The mean precipitation isotopes in TCs are markedly
lower than those in other tropical and summer precipitation[Lawrence, 1998; Lawrence and Gedzelman, 2003; Lawrence
et al., 1998, 2004]. Lawrence et al. [1998] speculated thatthe low precipitation isotope ratios in TCs result from theirhigh, thick clouds, large precipitation region, and relative
longevity. Because of continuing fractionation during condensation, the isotope ratios of water vapor decrease as
saturated air rises [Gedzelman and Lawrence, 1982], an
example of the rainout effect [e.g., Dansgaard, 1964]. They
also tend to be lower under thicker clouds, increases in the
precipitation efficiency [Lawrence and Gedzelman, 1996],
and downwind from a precipitation region.
[4] At the surface over land, studies have found that theisotope ratios of both the precipitation and water vapor inTCs decreased radially inward toward the eye [Lawrence
and Gedzelman, 1996; Lawrence et al., 1998, 2002]. The
following two factors likely explain these decreases: theinward increase of precipitation efficiency due to higher
cloud tops, and diffusive isotopic exchange between falling
droplets and the ambient water vapor. Because lighter
isotopes preferentially diffuse from condensates, the isotope
ratios of droplets become heavier as they fall. In contrast,
ambient water vapor is isotopically depleted in the heavier
isotopes, one of the rainout effects. Therefore the precipitation condensed from this water vapor with lighter isotope
ratios becomes isotopically lighter [Miyake et al., 1968].

D12113

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D12113Figure 1. Track of Shanshan from Best Track data for the period 10– 20 September 2006. Filled circles
represent positions of Shanshan at 0000 UTC, while crosses represent positions at 0300, 0600, 0900,
1200, 1500, 1800, and 2100 UTC on 15 and 16 September 2006.
Lawrence et al. [1998] showed that a two-dimensional
microphysical model with isotopic physical algorithms
developed by Gedzelman and Arnold [1994] simulated
idealized TC situations. The model calculated the inward
decreases in isotope ratios of precipitation and water vaporcaused by stepwise isotope exchange between falling precipitation and converging water vapor. Recently, Lawrence
et al. [2006] reported the isotopic observation at thesouthern coast of US, finding the slightly higher isotope
ratios of water vapor around the eye of Hurricane Katrina,
2005.
[5] In contrast to surface-based observational results,
isotope ratios of precipitation and water vapor collected
over the ocean at heights from 600 to 3000 m during flights
in Hurricane Faith, 1967, quickly increased to high values
in the eyewall [Ehhalt and Ostlund, 1970]. Gedzelman et al.
[2003] collected precipitation and water vapor during flights
into four hurricanes at flight levels between 850 and 475 hPa
and analyzed the stable isotopes. The lowest isotope ratios
occurred in or near regions of stratiform precipitation
between about 50 and 250 km from the hurricane center,but isotope ratios increased inward in the eyewall. The
occurrence of high isotope ratios in the eyewall suggeststhat a large fraction of the water vapor originates or isaltered deep within the hurricane, where air just above thesea surface is filled with sea spray with heavy isotope ratios[Black et al., 1986]. The results of a two-layer fractionationchamber model [Gedzelman et al., 2003] showed that sea
spray that filled the atmosphere [Wang et al., 2001] supplied
the eyewall with up to 50% of its water vapor and waslargely responsible for its high isotope ratios.
[6] Although previous isotopic observations have provided
much information, there is no isotopic ‘‘ground truth’’ thatshows the isotope ratios and d-excess of water vapor in a
TC eye during the intensification of a TC over the sea,accompanied by a sudden cessation of precipitation. This

may reflect either the coarse temporal interval of theoperational observations or the difficulty in capturing a
TC developing over subtropical seas, or both. We therefore
attempted intensive surface-based observations with hightemporal resolution of isotopes of both precipitation andwater vapor in a TC passing over Ishigaki Island, Japan,
during the passage of Typhoon Shanshan in mid-September
2006. We also made comprehensive meteorological observations so that we could analyze the features of the
precipitation pattern accompanying Shanshan and better
understand atmosphere moisture cycling in a TC developing
over the sea. Moreover, it is noteworthy that this is the firstreport to describe surface-based measurement of isotope
ratios and d-excess of water vapor in a TC eye over anisland small enough to have little effect on the storm.

2. Data and Methods
2.1. Isotopic Data
[7] Intensive isotopic observations were conducted from11 to 18 September 2006 at the Japan International Research Center for Agricultural Sciences (JIRCAS) on Ishigaki Island in southwestern Japan (Figure 1). Ishigaki Island
is a small subtropical island that is 221 km2 in area and is aconvenient location to capture a TC developing over thesubtropical sea.
[8] Precipitation samples were automatically collected forevery 1-mm amounts of precipitation with an auto-precipitation sampler. Water vapor was cryogenically collected at
liquid nitrogen temperature ( 196°C) using an extraction
line composed of a U-shaped glass tube filled with glass
beads [Sugimoto et al., 2002]. Air was introduced from an
air inlet on the roof of the building into the extraction line in
the laboratory of the JIRCAS through a polyethylene tube
using a vacuum pump positioned at the outlet of theextraction line. The air intake for the water vapor sampling

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D12113Figure 2. Record of (a) 30-min averaged surface pressure, (b) 10-min accumulated precipitation, (c) 30-min
averaged temperature (solid line) and relative humidity (broken line), (d) 10-min averaged wind speed(line) and direction (dots), and (e) salinity in precipitation samples collected at Ishigaki Island from1500 UTC on 14 September to 0300 UTC on 17 September 2006.
was adequately shielded from the precipitation. The flowrate of the air was reduced to about 300 mL min 1 forcomplete extraction of the water vapor. Sampling wascontinued until at least 0.3 mL of water was obtained; inother words, sampling duration depended on the mixing
ratio of the air sample, and was generally about 70 min in
our observations. At the end of sampling, carbon dioxidethat was trapped with the water vapor was vaporized andremoved by pumping out at liquid nitrogen ethanol slush
temperature ( 90°C). Water vapor samples were collectedaround 0430, 1030, 1630, and 2230 UTC every day.
[9] The isotopic composition of water samples was analyzed by the CO2/H2/H2O equilibration method using a
mass spectrometer at the Graduate School of Environmental
Science, Hokkaido University. Isotopic compositions are
expressed with values defined as dsample = (Rsample/RSMOW
1)  1000, where Rsample is the isotope ratio in the sample,
and RSMOW is the isotope ratio in the standard (i.e., standard
mean ocean water, SMOW). The d2H and d 18O values ofwater vapor and precipitation near sea level range fromabout +40 to 400 per mil and +5 to 50 per mil,respectively [Dansgaard, 1964]. Analytical errors were lessthan 2 per mil for d 2H and 0.15 per mil for d 18O, respectively. Deuterium excess (d-excess) was calculated as

8  d18O. The magnitude of d-excess
d-excess = d2Hdepends on several nonequilibrium processes [e.g., Craig,
1961; Merlivat and Jouzel, 1979]. The global average value
measured in precipitation is 10 per mil.
[10] We also measured the salinity of the collected
precipitation by a compact electric conductivity meter todetect the sea-spray content of the precipitation samples.
Sea spray, which has heavy isotope ratios, like ocean water
does, was trapped together with the falling droplet, causing
an overestimate of precipitation isotope ratios. We therefore
corrected the precipitation isotope ratios for sea spray
content, roughly assuming that the isotope content of sea
spray is 0 per mil as in ocean water. The correction equation
is written as d correct = d obs/(1 Sobs/Ssea), where d correct isthe corrected isotope content of the sample, d obs is theisotope content of the observed sample, Sobs is the salinityof the observed sample, and Ssea is the 3.4% salinity ofocean water. This equation to correct for precipitation
isotope ratios assumes that the salt derived from sea spray
drops without evaporation. The average amount of salinity
detected in precipitation samples was about 0.05%(Figure 2e). The largest amount of salinity, about 0.6%,
was detected in precipitation around the TC center, causing
about 1.0 per mil overestimation for d18O. The isotope

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Figure 3. Equivalent blackbody temperature (TBB) at
2100 UTC on 15 September 2006. The contour interval is
10 K. The cross marks the position of Ishigaki Island.
content of water vapor was not corrected because of theabsence of sea spray in the water vapor samples.
2.2. Meteorological Data
[11] As meteorological data, we observed 1-min accumulated precipitation and 30-min averaged surface pressure,surface wind, temperature, and relative humidity at JIRCAS. Surface wind data averaged over 10-min intervals
derived from the Automated Meteorological Data Acquisition System (AMeDAS) of the Japan Meteorological Agency (JMA) at Ishigaki were also used. The precipitation
pattern over Ishigaki Island was estimated from an operational weather radar map at Ishigaki site provided by the
JMA. The radar echo data have a horizontal resolution of
1.0 km. The precipitation pattern was derived from the
2A12 product of the Tropical Rainfall Measuring Mission
Microwave Imager (TRMM-TMI). The 2A12 data consistof instantaneous TRMM-TMI precipitation retrievals with ahorizontal resolution of about 5.1 km. Equivalent blackbody
temperatures (TBB) taken from satellite images collected by
the Geostationary Meteorological Satellite (MTSAT) werealso used in this study. These satellite data have a horizontal
resolution of 0.2° for both longitude and latitude.
[12] The track of Shanshan was obtained from the Best
Track data of the Regional Specialized MeteorologicalCenters (RSMC) Tokyo-Typhoon Center. The data set
consists of the names, positions, maximum surface pressure,and maximum wind speeds of TCs, recorded at 3-h intervals
around Ishigaki Island. Estimates of the 10-min positions of
the cyclone center were determined by spline interpolationof the 3-h data.

3. Results
3.1. Precipitation Pattern of Typhoon Shanshan[13] Figure 1 shows the track of Typhoon Shanshan
derived from the Best Track data. Shanshan was upgraded

D12113from a tropical depression to a tropical storm (maximum
10-min sustained wind speed in excess of 17.2 m s 1) at
1200 UTC on 10 September 2006, when situated at 16.8°N,
134.8°E. Shanshan moved westward and turned toward thenorth over the sea south of the Ishigaki Island on 14
September. Shanshan gradually increased in intensity over
the warm sea and passed between Iriomote and Ishigaki
islands at 2100 UTC on 15 September, with a centralpressure of 925 hPa and a maximum wind speed in excess
of 50 m s 1. During the passage over Ishigaki Island, an eye
approximately 30-km in radius became clearly visible in thesatellite image (Figure 3). At that time, Ishigaki Island was
located in the eye.
[14] Figure 2 shows a time series of surface observationsat Ishigaki Island, while Figure 4 presents a radar map
derived from the weather radar at the Ishigaki site. When
Shanshan was located over the sea about 300 km south ofIshigaki Island, two outer rainbands (referred to as OB1 andOB2) quickly passed over Ishigaki Island at 1920 UTC on
14 September (Figure 4a) and 0320 UTC on 15 September(Figure 4b), causing heavy precipitation (Figure 2b). The
precipitation accompanying these outer rainbands was characterized by heavy convective precipitation with subsequent
stratiform precipitation.
[15] After 0900 UTC on 15 September, as Shanshan
approached close to Ishigaki Island, easterly wind speed
gradually increased, and relative humidity remained high at
more than 90% (Figure 2c). The broad echo region spreading about 150 km from the eye, known as the rain shield[Shimazu, 1998], covered Ishigaki Island (Figure 4c),causing stratiform precipitation (Figure 2b). In the rain
shield, two inner rainbands (referred to as IB1 and IB2)
passed over Ishigaki Island (Figures 4d and 4e), causing
heavy convective precipitation around 1300 and 1600 UTC
on 15 September (Figure 2b). After IB2 had left, a ring ofintense convection surrounding the center, front eye wall(referred to as the FEW), began to cover Ishigaki Island at
1800 UTC.
[16] Although a power failure due to the storm interrupted
the weather radar observation after 1900 UTC on 15
September (Figure 4f), precipitation patterns associated with
Shanshan were provided by TRMM-TMI observations at
0440 UTC on 16 September (Figure 5). During the passageof the FEW over Ishigaki Island from 1800 – 2040 UTC on
15 September, heavy convective precipitation and strong
easterlies exceeding 45 m s 1 were observed at Ishigaki
Island (Figures 2b and 2d). At 2040 – 2130 UTC, when
Ishigaki Island was located in the weak echo region of theeye (Figure 5), there was a rapid shift to no or little
precipitation and wind speed weakened with veering. The
veering indicated that Ishigaki Island was to the right of thedirection of Shanshan’s movement. The lowest surfacepressure of 924 hPa was recorded at this time (Figure 2a),while surface temperature increased (Figure 2c).
[17] Strong westerlies reached about 50 m s 1 following
the passing of the eye (Figure 2d). The rear eye wall(referred to as the REW) brought the heaviest precipitation,
in excess of 10 mm in 10 min. After the passage of the
REW, the precipitation accompanying the rain shield ended
over Ishigaki Island by 0200 UTC on 16 September. The
wind speeds gradually decreased in association with thedeparture of Shanshan. As Shanshan moved away from

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D12113Figure 4. Radar map of the Ishigaki site at (a) 1920 UTC on 14, (b) 0320 UTC, (c) 1100 UTC, (d) 1300
UTC, (e) 1600 UTC, and (f) 1900 UTC on 15 September 2006. Light shading shows regions of echo
intensity of 10– 40 mm h 1, while darker shading indicates regions of echo intensity greater than 40 mm
h 1. Open circles indicate the position of Ishigaki Island.
Ishigaki Island, none of the outer rainbands passed overIshigaki Island.
[18] These meteorological observation results show that
our observations at Ishigaki Island captured the front,
central, and rear structures of Shanshan.
3.2. Isotopic Characteristics of Precipitation andWater Vapor[19] From 11 to 18 September 2006, 26 water vaporand 55 precipitation samples were successfully collected.
Figure 6 shows the time series of isotope ratios of precipitation and water vapor observed at Ishigaki Island, together
with their d-excess values. Although the water vapor
sampling was conducted at 6-h intervals, we also irregularly
carried out water vapor sampling from 2020 – 2130 UTC on
15 September during the passage of the eye. Unfortunately,a deficiency of liquid nitrogen due to a power failure
interrupted the water vapor sampling from 1630 UTC on
16 September to 0430 UTC on 17 September.
[20] The isotope values of water vapor showed a large
range. The isotope ratio gradually decreased from 13 permil at 2230 UTC on 14 September to 24 per mil at
1630 UTC on 15 September. An anomalously high isotope
ratio of 13 per mil appeared at 2100 UTC on 15
September. After 0430 UTC on 16 September, isotope ratios
of about 16 per mil for water vapor remained steady. The

Figure 5. Surface precipitation map derived from TRMMTMI at 0440 UTC on 16 September 2006. Regions of echo
intensity of 4 – 7 mm are shown by light shading, while
regions greater than 7 mm are indicated by heavier shading.
The contour interval is 3 mm. A solid line and closed circles
represent the position of Ishigaki Island in relation to the TC
center.

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D121131600 UTC on 15 September, while it quickly decreased
from 10 to 0 per mil after 1600 UTC. Figure 7 shows ascatterplot of the d 2H and d 18O values of water vapor andprecipitation. The samples plotted around the meteoric
water line (MWL) [Craig, 1961].
[22] In general, as precipitation continues falling, theisotope ratios of precipitation decrease with increasing precipitation totals, i.e., the so-called amount effect [Dansgaard,1964]. However, as shown in the isotopic observational
results, the variability in the isotope ratios of the precipitationaccompanying Shanshan cannot be convincingly explainedby the amount effect.

4. Discussion
Figure 6. Record of (a) d 18O and (b) d-excess of precipitation (crosses) and water vapor (closed circles with solid line)from 1500 UTC on 14 September to 0300 UTC on 17
September 2006. These isotope ratios of precipitation werecorrected for sea-spray content.
d-excess of water vapor gradually decreased with a minimum of about 11 per mil at 2100 UTC on 15 September.
[21] The isotopic values of precipitation, which werecorrected for sea-spray content, also had a large range. In
OB1 and OB2, the isotope ratios of precipitation quickly
decreased with significant amplitude by more than 5 permil. From 1000 UTC on 15 September during the passageof the rain shield over Ishigaki Island, precipitation isotope
ratios gradually decreased from 7 to 13 per mil. Abruptchanges in the precipitation isotope ratios occurred at 1230
and 1530 UTC around the passage of IB1 and IB2. The
precipitation isotope ratios slightly increased around 1200
and 1800 UTC. Unfortunately, the precipitation samples in
the FEW from 1900 to 2100 UTC were not collected. It isremarkable that anomalously high precipitation isotope
ratios occurred in the REW around 2200 UTC on 15
September; d 18O values of about 6 per mil were as highas those of OB1 and OB2. After the passage of the REW,
the isotope ratios in the little precipitation that occurred
decreased to 13 per mil at 0330 UTC and increased to
7 per mil at 0800 UTC on 16 September. The d-excess of
precipitation of around 10 per mil slightly decreased until[23] The isotopic ratios of precipitation and water vapor
in Shanshan exhibited systematic variation with the radial
distance from the TC center. Figure 8 shows the radial
profile of d18O and d-excess of precipitation and water
vapor observed at Ishigaki Island. The situation in which theobservation site was located on the northern (southern) sideof Shanshan and Shanshan approached (moved away from)
Ishigaki Island is referred to as the front (rear) side ofShanshan, hereafter.
[24] Between 80 and 300 km radius from the position ofOB2 to IB2 in the front side (referred to as the TC’s outerregion), a clear inward decrease in the isotope ratios ofwater vapor appeared. The gradient, which is defined as thechange in the isotope ratios to the radial distance, waslargest in the area outer part of the rain shield in the front
side, between 80 and 160 km in radius. In contrast, an
inward increase in isotope ratios of water vapor was
significant around the eye and eye wall (referred to as theTC’s inner region). On the other hand, precipitation isotope
ratios gradually decreased inward in the TC’s outer region.
In the TC’s inner region, anomalously high isotope ratios ofprecipitation appeared in the REW.
[25] We speculate that the observed isotopic variation can
primarily be attributed to moisture cycling in the boundary
layer. TC-relative winds are divided into two components
depending on the wind direction: the tangential wind thatflows parallel to curved isobars with velocity defined as
positive counterclockwise, and the radial wind that flows
toward its center across the isobars with velocity defined as

Figure 7. Scatterplot showing d 2H and d 18O for precipitation (crosses) and water vapor (closed circles
with line) at the (a) front and (b) rear sides of the TC. The broken lines denote the meteoric water line.
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D12113Figure 8. Radial profile of (a) 10-min precipitation (filled bar), d18O and (b) d-excess of precipitation(crosses) and water vapor (closed circles with line). Positive (negative) distance shows the conditions on
the front (rear) side of the moving TC. The shaded region in the middle indicates the region of noobservations.
positive inward. These winds were derived from the 30-min
averaged surface wind observed at JIRCAS, although thewind was not recorded after 1900 UTC on 15 September.
Figure 9 shows the radial profile of two wind components.
The radial wind increased inward in the TC’s outer region.
In the TC’s inner region, the radial wind decreased inward,
while the tangential wind quickly increased inward. Thissuggests that inward flow was conspicuous in the TC’souter region, whereas relatively weak inward flow and highwinds occurred in the TC’s inner region.
[26] Isotopic observational results clearly show that the
inward decreases in the isotope ratios of water vapor andprecipitation appeared in the TC’s outer region, where
inward flow was conspicuous. The largest gradient was in
the precipitation region of the rain shield when the water
vapor passed through regions of precipitation. The inward
decrease in isotope ratios of water vapor in the TC’s outerregion was mainly caused by the rainout effect which
involves both condensation efficiency as reflected in inwardly increasing cloud thickness and isotopic exchange
between falling droplets and ambient water vapor. In active
rainout effect, as air masses move through a precipitation
region, heavier isotopes are progressively depleted as the
air masses lose moisture (e.g., the ‘‘continent effect’’)[Dansgaard, 1964]. In this case, the water vapor was
isotopically depleted through the organized precipitation
region of Shanshan. Water vapor content would not havedecreased due to the radial inward convergence [e.g.,
Kurihara, 1975]. The precipitation in the TC’s outer region
was isotopically depleted stepwise by the inward decreases
in the isotope ratios of water vapor.

[27] On the other hand, anomalously high isotope ratiosof water vapor occurred in the TC’s inner region where
inward flow was relatively weak and surface wind velocity
was high. Figure 2e shows the salinity in collected precipitation samples. The salinity was anomalously high aroundthe TC center, indicating that sea spray filled the atmosphere due to the high winds over the sea surface. Underhigh winds and the resulting extensive formation of sea
spray, the surface area of liquid water of sea spray andsea surface exposed to water vapor increases tremendously.
Sea spray, which has heavy isotope ratios like those ofocean water, underwent diffusive isotopic exchange withwater vapor before falling back to the sea surface, resulting
in the offset the radially inward decrease of isotope ratios.
Also the evaporation from the sea surface caused the heavy
isotope ratios in water vapor. We refer to these effects as‘‘isorecharge’’. Because of limitations of the observationaldata, quantitative understanding of the two kinds of isorecharge remains unclear. However, in the TC’s inner
region, weak inward flow weakened the rainout effect andthe impact of the isorecharge became significant, causing
the anomalously high isotope ratios of the water vapor. The
precipitation in the eye wall was also isotopically enrichedby the water vapor with heavy isotope ratios.
[28] Another remarkable change in the isotopic composition during the passage of Shanshan was the decrease in thed-excess of both precipitation and water vapor in the TC’s
inner region. The physical processes that affect d-excess areevaporation and diffusive water vapor change in subsaturated air, while the production of precipitation from water
vapor essentially conserves the d-excess. The d-excess

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Figure 9. Radial profile of radial (solid line) and tangential(broken line) winds derived from 30-min averaged surface
winds observed at Ishigaki Island.
of evaporated vapor from the water surface decreases(increases) as the relative humidity of surface air increases(decreases) [Craig and Gordon, 1965]. Moreover the dexcess of water vapor that undergoes diffusive isotopic
exchange with sea spray decreases. Therefore the lower dexcess of water vapor in the TC’s inner region can be
attributed to the intensive isotopic exchange between water
vapor and liquid water, given the TC’s high relative humidity of more than 90% (Figure 2c). A unique circumstance ofa TC is the intensity of isotopic exchange between water
vapor and liquid water of sea spray and sea surface withalmost saturated surface air and high winds, leading toanomalously high isotope ratios and low d-excess valuesof water vapor in the TC’s inner region.
[29] Interestingly, there were short-term variations inprecipitation isotope ratios within individual rainbands.
Precipitation isotope ratios accompanying the outer rainbands OB1 and OB2 spatially decreased with significant
amplitude (Figure 8). In the front side of the TC, outerrainbands quickly moved, causing convective precipitation
with subsequent stratiform precipitation over Ishigaki Island.
Since condensation in the convective region reduces theisotope ratio of the water vapor in saturated rising air byremoving the heavy isotopes as precipitation [e.g., Gedzelman
and Lawrence, 1990; Gedzelman and Arnold, 1994], theisotope ratios of remaining water vapor in the subsequent
stratiform region become lighter, causing precipitation isotope ratios to decrease both downwind and with time
(Figures 6 and 8), one of the rainout effects [Gedzelman
and Lawrence, 1982]. On the other hand, during the passageof the inner rainbands IB1 and IB2, short-term changes inprecipitation isotope ratios had high variability. A shortterm isotopic variability in the rain shield is expected
depending on the trajectory taken by each air parcel as it
travels through regions of convective and stratiform precipitation. Detailed trajectories are needed and this may not be
possible without suitable meteorological data and numericalsimulation data to obtain the trajectories. Such complex
moisture cycling in the multiple clouds of TCs should beconsidered in future studies.

5. Summary[30] Isotope ratios of precipitation and water vapor during
the passage of Typhoon Shanshan were observed at Ishigaki

D12113Island, Japan. Isotopic observations at observational intervals of 6 h for water vapor sampling and 1-mm amounts ofprecipitation for precipitation sampling allow for a better
qualitative understanding of the atmospheric moisture cycling of TCs. Observational results are summarized asfollows: the isotope ratios of both precipitation and water
vapor decreased radially inward in the TC’s outer region;
anomalously high isotope ratios of both precipitation andwater vapor appeared in the TC’s inner region; and thed-excess of both precipitation and water vapor tended todecrease in the TC’s inner region.
[31] Figure 10 illustrates the moisture cycling in a developing TC that controls the observed isotopic features withthe radial distance from the TC center. In the TC’s outerregion, where inward flow was conspicuous in the boundary
layer, the water vapor was isotopically depleted due to therainout effect which involves both condensation efficiency
as reflected in inwardly increasing cloud thickness andisotopic exchange between falling droplets and the ambient
water vapor. In the TC’s inner region, where inward flow
was relatively weak and surface wind velocity was high,water vapor was isotopically enriched by weak rainout
effect and intensive isorecharge from sea spray and sea
surface with heavy isotope ratios. Since water vapor mainly
acts as a source of precipitation, the isotope ratios ofprecipitation also had systematic variation. A unique circumstance of a TC is the intensity of isotopic exchange
between water vapor and liquid water of sea spray and sea
surface with almost saturated surface air and high winds,leading to anomalously high isotope ratios and low d-excess
values in the TC’s inner region.
[32] These isotopic observational findings indicate asignificant possibility of differences in moisture cycling
between the inner and outer regions of a TC developing
over the sea, although we still need to verify the possibility
quantitatively by using numerical models on the water
budget in a TC [e.g., Braun, 2006], for example. Future
work will involve the development of a mesoscale isotopic
model to realistically simulate the isotopic features observedin Shanshan and quantitatively discuss the moisture cycling
related to the intensification of TCs over the sea.

Figure 10. Schematic cross section of moisture cycling ina developing TC. Solid arrows indicate trajectories ofisotopically heavier water vapor, while open arrows indicate
trajectories of isotopically lower water vapor. Filled circles
represent sea spray.

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D12113FUDEYASU ET AL.: ISOTOPE RATIOS OBSERVED IN TYPHOON[33] Acknowledgments. We are grateful for the assistance of many
scientists at the Japan International Research Center for Agricultural
Sciences. Thanks are also extended to the Japan Meteorological Agency
for supplying meteorological data on Typhoon Shanshan. This work was
supported by a Grant in Aid for Young Scientists, (B) 18740302, from the
Ministry of Education, Sports, Culture, Science, and Technology, Japan.
Additional support has been provided by the Instutite of Observational
Research for Global Change, Japan Agency for Marine-Earth Science andTechnology.

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