It Process
Resume:
Chinese Science Bulletin
Sea surface temperature record from the north of the
East China Sea since late Holocene
LI GuangXue1,2, SUN XiaoYan3, LIU Yong1, BICKERT Torsten4 & MA YanYan1
1
College of Marine Geosciences, Ocean University of China, Qingdao 266100, China;
2
Key Laboratory of Submarine Geosciences and Prospecting Techniques, Ministry of Education, Qingdao 266100, China;
3
National Marine Data and Information Service, Tianjin 300171, China;
4
Department of Geoscience, University of Bremen, Bremen 28359, Germany
k
Using the alkenone paleotemperature index U 3 7, a high-resolution sea surface temperature (SST)
record since 3600 a BP was reconstructed from the mud area in the north of the East China Sea. Com-
bining with the grain size distribution curve of sensitive grain size group, which may reflect the East
Asia Winter Monsoon activity, the palaeoenvironmental evolution cycle throughout the late Holocene in
the area was obtained. The marine environment evolution during the last 3600 years displays a
five-stage trend. (1) Temperature descending period from 0.85 cal. ka BP to present. The maximum
temperature decrease amplitude is 2 . The winter monsoon intensified and Little Ice Age were rec-
orded in this period. (2) Warming period from 1.90 to 0.85 cal. ka BP. The mean temperature increase
amplitude is 0.8 . The Sui-Tang warming period was recorded at about 0.85 1.35 cal. ka BP and a
prominent cooling event was recorded at 1.4 cal. ka BP in this period. (3) Temperature descending pe-
riod from 2.55 to 1.90 cal. ka BP. Temperature cooling amplitude is 0.9 . This period is coincident with
an integrated temperature circle recorded in the Antarctic ice core, with the temperature changes from
a slow cooling stage to a rapid warming stage. (4) Temperature comparatively stable with a little as-
OCEANOLOGY
cending period from 3.2 to 2.55 cal. ka BP. Temperature warming amplitude is 0.3 . This period is
coincident with the temperature fluctuant ascending period recorded in Antarctic ice core. (5) Temper-
ature comparatively stable with little descending period from 3.6 to 3.2 cal. ka BP. This period corres-
ponds with the temperature fluctuant cooling period recorded in Antarctic ice core. Basically, those five
periods were coincident with the Antarctic ice core record. During the global cooling stage, the SST
change in the continental shelf sea can be adjusted simultaneously.
k
north of the East China Sea, mud area, U 37, SST, global change
The mud area in the north of East China Sea was af- tem evolution and climatic changes resulting from varia-
fected by two current systems, the Yellow Sea Coastal tions of meridional heat flux. Sediment grain size has
Current which is controlled by East Asia Winter Mon- been used as an index to indicate fluid dynamic intensity,
and is extensively used in loess and lacustrine research[2].
soon, and the Yellow Sea Warm Current which is de-
rived from Kuroshio Current. The study area deposits Sensitive grain size group is also studied in the conti-
with swirl mud continually, which came into being since nental shelf sea. The result shows that the change of par-
the last High Sea Level period (about 7 cal. ka BP)[1]. It ticle size is an effective proxy to conclude the intensity
is a sensitive area to the environmental change, and has
Received November 5, 2008; accepted February 26, 2009; published online May 25, 2009
high potential information on the identification of the doi: 10.1007/s11434-009-0231-2
Corresponding author (email: *******@***.***.**)
climatic oscillations that occurred during the Holocene. Supported by the National Basic Research Program of China (Grant No. 2005CB-
SST may provide direct evidence of marine current sys- 422304)
Citation: Li G X, Sun X Y, Liu Y, et al. Sea surface temperature record from the north of the East China Sea since late Holocene. Chinese Sci Bull, 54: 4507 4513, doi:
10.1007/s11434- 009-0231-2
of the coastal current induced by the East Asia Mon-
soon[3,4].
The sea surface temperature (SST) record from the
k
mud area in the north of East China Sea using U 3 7 me-
thod has been reconstructed in this paper. Combining
with the variety of sensitive grain size group, the marine
environmental evolution process throughout the late
k
Holocene will be discussed. The U 3 7 index is less sus-
ceptible to diagenesis, organism dissociation, salinity
and nutrient availability. So the unsaturated ketone can
k
be preserved perfectly in the marine sediment. U 3 7 and
k
SST value have a stable correlation. Therefore U 3 7-SST
method has been widely used in a variety of areas, such
as the whole marine sediments and lacustrine sedi-
ments[5 8], but until now there has been no publication
on the East China Sea.
k
The U 3 7 index is converted on the relative abundance
of the diunsaturated (C37:2), triunsaturated (C37:3) and
tetraunsaturated (C37:4) methyl ketones of 37 carbon at- Figure 1 Location of core FJ04 and main currents in the East
k
oms. The definition is U 3 7=(C37:2-C37:4)/(C37:2+C37:3+
[10]
China Sea (modified from Yuan et al. ). TWWC-Taiwan warm
current; YSWC, Yellow Sea warm current; YSCC, Yellow Sea
C37:4). In the open marginal oceans, these compounds coastal current.
are biosynthesized by some Haptophyceae algae, the
1.2 Alkenone analysis
coccolithophorid Emiliania huxleyi being the main pro-
ducer[9]. The Emiliania huxleyi lives widely in all the Alkenone test was performed in Organism Extraction
and Chromatograph Analysis Labs in Marine Geology
present oceans including tropical and polar waters.
Group of Bremen University. The procedures and
However, the C37:4 alkenone is rarely detected from low-
equipment used for the analysis of C37 alkenones have
to mid-latitudes marine sediments and only becomes
been detailed by Stuiver et al.[11]. Briefly, there are three
abundant when temperature is very low (
steps. Firstly, sediment samples were freeze-dried and
k
U 3 7 index can be usually simplified for the following
manually ground for homogeneity. The dry subsample
k
expression: U 3 7 = C37:2/(C37:2+C37:3).
(ca. 3 g) was used to extract three times separately with
methonal, methonal:dichloromethane = 1:1 and dich-
1 Sampling and testing
loromethane liquor in an ultrasonic bath. Then the
1.1 Sampling blending sample was separated in a centrifugal machine
to absorb the floating liquid. The liquid was desalted,
The fine sediment sample is from core FJ04, which was
dried over Na2SO4, concentrated under N2. Secondly,
collected using gravity sampling pipe during the summer
specification was performed using KOH (0.1 N) in me-
cruise for National Keystone Basic Research Program
thanol at 80 for 2 h, and then the neutral fraction
Marine physical environmental change and climate
containing the alkenones was obtained by partitioning
response in the East China Sea in June 2006. The vessel
into hexane. Finally, the extracts were analyzed by cap-
is Dongfanghong No. 2 of Ocean University of China.
illary gas chromatography using a HP 5890A gas chro-
The core was airproof immediately in order to avoid the
matograph equipped with a 50 m 0.32 mm fused silica
surface sediment dissipation. The water depth of core
column, and flame ionization detection (FID). Helium
FJ04 (31.68 N, 125.81 E) is 67 m, and its length is 167
was used as carrier gas. The oven temperature was pro-
cm (Figure 1). It was cut into 83 slices with 2 cm inter-
grammed from 50 to 150 at 30 /min, from 150 to
val in laboratory, 63 of which were used to do alkenone
230 at 8 /min, from 230 to 320 at 6 /min, and
analysis.
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the final temperature was maintained for 45 min. temperature reconstruction in our study area, three dif-
ferent equations calculating the modern SST based on
1.3 Chronology k
the U 3 7 of the surface layer sediment of core FJ04 were
The chronology of core FJ04 was performed at Guang-
compared (Table 2). By comparison, it was found that
zhou Geochemistry Institute of the Chinese Academy of
all the three SST reconstructions are close to the mea-
Sciences and National Key Lab of Nuclear Physics and
surement SST with an annual mean value of 19.78
Technique, Peking University. The material used for
(Figure 2(a)). (1) The SST from Prahl et al. s[15] equation
chronology was the benthonic foraminifera A. compres-
based on algae culture gives an error value of 0.57
siuscula with the diameter larger than 63 m. The three
lower than the modern SST[16] (Figure 2(a)). (2) The
uncorrected 14C ages were converted to the calendar
SST from Pelejero et al. s[14] equation based on the top
ages using the international universal software Calib
of cores from the South China Sea gives an error value
5.02[12]. The age model was constructed by linear inter-
of 0.43 lower than the modern SST. (3) The SST
polation between different AMS 14C dates, and then the
from M ller et al. s[13] equation based on ocean surficial
deposition rate and sample resolution were calculated
sediments of 370 sampling points from 60 N to 60 S
(Table 1). Table 1 shows that the deposition rate varied
gives an error value of 0.14 lower than the modern
significantly. The deposition rate in 1 1.54 cal. ka BP
SST. Thus it can be seen that the errors for all the three
was much faster than in the early and later stages. The
calibrations are less than 3%, while the global equa-
highest sample resolution can reach 8.7 a/cm.
tion[13] is the most suitable one with the error less than
0.7%.
14
Table 1 AMS C age and sample resolution in Core FJ04
AMS 14C age Calendar age Deposition rate
Depth Resolution
(cm) (a BP) (cal. a BP) (cm/ka) (a/cm) k
Table 2 Comparison of the estimation SST from different U37 cali-
1279 32 997 39.1 25.5
38 40
brations with the measured modern SST
185*-**-**** 114.2 8.7
100 102 k
SST from the U 3 7 (=0.69) of the core top
Equation
326*-**-**** 37.75 26.5
153 155 k [15]
19.21, 0.57 lower than modern SST
U 37 =0.039+0.034 SST
k [14]
19.35, 0.43 lower than modern SST
U 37 =0.092+0.031 SST
1.4 Grain size analysis k [13]
19.64, 0.14 lower than modern SST
U 37 =0.044+0.033 SST
Grain size analysis was performed by using Malvern
Accordingly, the equation proposed by M ller et al.[13]
2000 laser instrument at the Key Lab of Submarine
was used to reconstruct the annual paleo-SST since 3600
Geosciences and Prospecting Techniques of Ministry of
OCEANOLOGY
years recorded in core FJ04. The SST values range from
Education in Ocean University of China. The measure-
19.5 to 22.7, with the variability exceeding 3.2 . The
ment range of the instrument is 0.02 2000 m, the
highest temperature was 22.7 which was recorded at
grain size resolution is 0.01, and the repeated mea-
1.01 cal ka BP, while the lowest temperature was 19.5
surement error is lower than 3%. Samples were pre-
which was recorded at 0.3 cal. ka BP. In view of marine
processed with excess H2O2 for 24 h to remove organ-
physical environmental characteristics, the factors that
ism. Hydrochloric acid was not used to release carbonate,
could cause SST change since the last 3.6 ka mainly
because one of the main sediment sources in the study
include: (1) Solar insolation changes caused by the
area was from the Huanghe River which contained a lot
change of earth orbit parameters. (2) Meteorological
of granule carbonate grain. The biogenesis component
factor. The northward winter monsoon dominates the
(mainly >63 m foraminifera shell) in the sediment was
area during wintertime, this cold air current reduces the
low with a mean content of less than 0.3% in the top 150
SST, and the quantity of heat dissipates because of the
cm of the core.
evaporation process. Its mechanism is coupled with the
effect of the coastal current. (3) Change of oceanic heat
2 Results and discussions
transportation, which is strongly related to strength or
k
Different equations to convert U 3 7 into SST have been weakness between the Yellow Sea coastal current and
proposed in different study areas[13 15]. But there is no the Yellow Sea warm current.
equation proposed for the East China Sea. In order to The reconstructed SST (Figure 3(a)) versus age over
evaluate a most suitable calibration formula for palaeo- the last 3600 years was plotted in comparison with the
Li G X et al. Chinese Science Bulletin December 2009 vol. 54 no. 23 4509
Figure 2 Annual mean SST (a) and winter time mean SST (b) distribution in the East China Sea. SST data measured for 50 years from Li et
[16]
al. . Winter time is the period of October to the next May when the East Asia northward monsoon was intensified.
k [18]
Figure 3 SST based on U37 record (a) and mean grain size of sensitive grain group (11 63 m) (b) for the core FJ04 together with air
[19] [20] 18
temperature anomaly reconstructed by Zhu (c), estimations of northern hemisphere mean SST variations from Moberg et al. (d), Oice
[21] [17]
of the Byrd ice core, Antarctica from Koutavas et al. (e), and the summer insolation at 32 N for the last 3.6 ka (f).
summer insolation changes at 32 N[17], the mean grain record curve is in the late stage of the last interglacial.
size curve of sensitive grain size group (Figure 3(b)) in High frequency cooling events on the SST curve show
core FJ04[18] and the air temperature anomaly curve that SST was influenced by Milankovitch forcing as a
(Figure 3(c)) from Zhu[19]. The change of summer inso- whole. The summer insolation at this latitude is low
lation is the background of temperature variance. Insola- since 1 cal. ka BP, which is coincident with the SST
k
profile reconstructed by U 3 7, the Northern Hemispheric
tion calculated from orbital parameters indicates that the
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SST[20] (Figure 3(d)), the Antarctic ice core record[21] sensitive grain size group also displays a high value.
(Figure 3(e)) and the air temperature curve proposed by Those features indicate that winter monsoon was ob-
Zhu[19]. This phenomenon indicates that the Milanko- viously intensified in the period[14], and the influence of
vitch parameter is the fundamental factor that controls Yellow Sea coastal current on the study area was also
the global change in a long cycle. strengthened. The air temperature profile of the East
The study area was controlled by both the cooling China reconstructed by Zhu also displays an obvious
Yellow Sea coast current water and the warm Yellow cooling stage during this period. Moberg et al.[20] studied
Sea warm current water (Figure 2(b)). The temperature SST record in the Northern Hemisphere synthetically,
in the north Yellow Sea is about 5 colder than in the and found that SST declines obviously since 850 a BP,
study area, so the cooling water transported by the with the lowest value at 450 a BP. Similar result occurs
coastal current can affect the area severely when the in core FJ04 record, with the lowest value at 300 a BP.
northward monsoon prevails. It can be concluded that The same information was also reported by Koutavas et
al.[21]. In addition, the Little Ice Age was recorded from
the SST variation reflects the prevailing relationship
between the coastal current controlled by the East Asia 500 to 100 a BP with two pronounced cooling events at
Monsoon and the Yellow Sea warm current. Li et al.[16] about 150 and 300 a BP. The maximum cooling ampli-
studied the water masses monthly variation in the East tude at 300 a BP was 2, same as Mg/Ca record of Lit-
China Sea based on water masses intensity index recon- tle Ice Age in the Caribbean Sea at 1699 1703 AD re-
structed by sea water temperature and salinity data. That
ported by Watanabe et al.[22].
study indicated that the northward East Asia Winter
(ii) Warming period from 1.90 to 0.85 cal. ka BP.
Monsoon began to appear in late September, streng-
The SST curve shows that the temperature in this period
thened in October, weakened next April and disappeared
was high, with four changing cycles containing three
in June. The Yellow Sea coastal current is controlled by short cooling events (about 50 years). Temperature in-
the northward monsoon for eight months in a year. As
crease amplitude was 0.5 1 with a mean value of
winter monsoon strengthened, the principal axis of the
0.8 . Rapid fluctuation occurs in the sensitive grain
cooling coastal current extended to the east (Figure 2(b)).
size, which indicates the influence of the East Asia Win-
Accordingly, the influence of cooling water masses
ter Monsoon and the Yellow Sea Coastal Current in a
transported by coastal current to the position of core
short cooling event. The reliability of the Sui-Tang
FJ04 must be intensified. Both of the cooling water
OCEANOLOGY
warming period (600 1000 AD) which was proposed
masses intensification and winter monsoon strengthen-
by Zhu[19] and the Dark Ages warming period (900
k
ing result in the SST decrease. The annual U 3 7-SST
1300 AD) in China have been the focus of argument.
cooling period in core FJ04 indicates that the winter
Based on the SST record of core FJ04 and the compari-
monsoon and Yellow Sea coastal current were intensi-
son with Antarctic ice core[21], the Sui-Tang warming
fied, while the warming period indicates that the winter
period was clearly recorded in the East China Sea se-
monsoon and Yellow Sea coastal current weakened.
diment, but the response time was in 0.85 1.35 cal. ka
When the coastal current in wintertime was indentified,
BP (comparatively 650 1150 AD). Two short cooling
the carried particles would become coarser. So the varia-
tion of mean grain size of sensitive grain size group[18] events were recorded in this period. The temperature
peak value occurs at 1.01 cal. ka BP. Meanwhile, SST in
can reflect the magnitude of coastal current driven by
the Northern Hemisphere also shows the warming trend.
winter monsoon.
The Dark Ages warming period was not recorded in core
By careful comparison, the SST record of FJ04 coin-
FJ04. A prominent cooling event was recorded at 1.4 cal.
cides well with the SST curve of the Northern Hemis-
ka BP, which is coincident with the cooling period in
phere (Figure 3(d)) and the Antarctic ice core record
Antarctic ice core record and the Northern Hemispheric
(Figure 3(e)). The SST curve of core FJ04 displays a
SST. This cooling event also occurred in three cave sta-
five-stage trend.
lagmites of southwestern China[23]. The cooling event
(i) Cooling period from 0.85 cal. ka BP to present.
was also displayed on Zhu s curve with a large time dis-
SST declined obviously in this period, with the maxi-
crepancy. The warming trend from 1.6 to 1.9 cal. ka BP
mum decrease amplitude of 2 . Mean grain size of
Li G X et al. Chinese Science Bulletin December 2009 vol. 54 no. 23 4511
semi-enclosed marginal sea and open ocean. It was found
may be related to the influence of the warming peak at
by carefully comparing that the SST change phases in the
1.9 cal. ka BP in Antarctic ice core record (Figure 3(e)).
continental shelf sea were not simultaneous with Antarctic
(iii) SST descending period from 2.55 to 1.90 cal. ka
ice core record. This difference may result from the dating
BP, with cooling amplitude of 0.9 . It coincides with
precision. Recently, the influence of carbon reservoir on
an integrated climate cycle accompanied with the tem-
14
C age in the East China Sea has not been clear. Moreo-
perature change of slow cooling to rapid warming rec-
ver, the 14C ages of core FJ04 were dated using the ben-
orded in the Antarctic ice core. Two comparatively
thonic foraminifera which lag generally behind the water
strong cooling events were recorded at 2.1 and 2.4 cal.
age from the planktonic foraminifera.
ka BP. The temperature recorded in Zhu s curve was
higher during this period. But a slight decrease trend still
3 Conclusions
occurred (Figure 3(c)). Sensitive grain size response to
the cooling event at 2.1 cal. ka BP occurs. k
U 3 7 method was used to reconstruct the palaeo-SST
(iv) Comparatively stable SST with little ascending
change of the mud area in the north of the East China
from 3.2 to 2.55 cal. ka BP. The warming amplitude was
Sea. By comparison, the global temperature equation
about 0.3 . It is coincident with the temperature fluctu-
proposed by M ller et al. was suitable for SST conver-
ation recorded in Antarctic ice core. Sensitive grain size k
sion in the study area. The result shows that the U 3 7 is a
curve is sensitive to such small climate fluctuations. A
usable proxy for SST reconstruction in the continental
pronounced cooling event was recorded at 3.2 cal. ka BP
k
shelf sea. The U 3 7-SST change curve displays a good
on the Zhu s temperature curve, other continental pa-
relationship with both the Antarctic ice core record and
laeo-climatic curves also recorded this event[24,25]. But
SST in the Northern Hemisphere.
there was no record in this study area.
The Yellow Sea coastal current driven by the East
(v) Comparatively stable SST with little descending
Asia Winter Monsoon controlled the SST of the study
from 3.6 to 3.2 cal. ka BP. It is coincident with the fluc-
area heavily. By comparison with the Antarctic ice core
tuant cooling period recorded in Antarctic ice core. SST
record, SST of the Northern Hemisphere, the variety of
decreases only about 0.3, which is opposite to Zhu s
mean grain size of sensitive grain size group, Zhu s air
curve. The Qinghai Lake record[26] controlled by winter
temperature anomaly curve, the land lacustrine and sta-
monsoon indicates that the climate was cold and dry
lagmite record, the SST change in the study area since
since 4 cal. ka BP.
3.6 cal. ka BP can be divided into five stages. (1) Cool-
The SST change in the continental shelf sea has a good
ing period from 0.85 cal. ka BP to present. The winter
response relationship with global climate change by
monsoon was intensified in this period. The Little Ice
comparing the SST record in the northern East China Sea
Age occurs with two cooling events at about 150 and
with the records from the Antarctic ice core and Northern
300 a BP. The maximum cooling amplitude of SST is
Hemisphere Ocean. The result shows that the flowing
2, which is coincident with the cooling amplitude of
marine water is sensitive to the global climate change.
Caribbean Little Ice Age . (2) Warming period from
Some good relationships occur. (1) The five stages since
1.90 to 0.85 cal. ka BP, with temperature increase am-
3600 a BP were coincident with the climate cycle in the
plitude of 0.5 1 and mean value of 0.8 . The Sui-
Antarctic ice core record. (2) Global climate cooling
Tang warming period was recorded at about 0.85 1.35
processes were usually stable and slow, and the SST can
be adjusted in time, for example some cold points rec- cal. ka BP. A prominent cooling event was recorded at
orded in SST curve of the study area are simultaneous 1.4 cal. ka BP, which also was recorded in the three sta-
with the Antarctic ice core curve during (i), (ii), (iii). (3) lagmite curves in the southwestern area of China. (3) Tem-
Global warming processes were usually comparatively perature descending period from 2.55 to 1.90 cal. ka BP
fast and unstable. In addition, no global climate warming with the cooling amplitude of 0.9 . This period is coin-
due to the greenhouse effect since the Industrial Revolu- cident with an integrated climate cycle as slow cooling
tion occurs in the study area. The SST change in the to fast warming recorded in the Antarctic ice core. (4)
Northern Hemisphere Ocean is simultaneous to the green- SST comparatively stable period with little ascending
house effect, which indicates the difference between from 3.2 to 2.55 cal. ka BP with the warming amplitude
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ARTICLES
of 0.3 . It is coincident with the temperature fluctuant climate change information in the future.
ascending process recorded in Antarctic ice core. (5) By analyzing those climate curves, the result shows
SST comparatively stable with little descending from 3.6 that the response of the continental shelf sea SST to the
to 3.2 cal. ka BP and the cooling amplitude of 0.3 . global climate is regular, but not simultaneous some-
Sediment grain size change is sensitive to the marine times. The five stages divided in the north of the East
dynamic intensity. The grain size curve change does not China Sea are coincident with the Antarctic ice core
go along with the temperature curve sometimes. It indi- record. Global climate cooling process was usually sta-
cates that the study area may be controlled sometimes by ble and slow. The SST change in the continental shelf
the South signal such as typhoon. So it is necessary to sea can be adjusted simultaneously. Global warming
consider more driving forces in order to identify the process was comparatively fast and unstable.
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