With the data, which were obtained from the SeaWinds scatterometer on board the National Aeronautics and Space
Administration (NASA) QuikSCAT satellite (12.5km*12.5km available from 1999 to current daily orbit swath), the
China offshore region were studied (105-135° E 15-45° N). Because swath location is not fixed, interpolation was
applied to get a fixed grid with 0.1° resolution. We calculate and analysis China offshore wind resources effective density
of wind energy (EDWE) at 10 meters high above the sea level. And find that EDWE is rich in offshore area. The highest
EDWE is in Taiwan Strait and North and South of the strait, with the EDWE 600-800W/m2, the next highest is East
China Sea and South China Sea. The lowest EDWE is Yellow Sea and Bohai bay, less than 400W/m2. And several other
wind energy resource-rich areas are: 1)the north of Bohai Bay, with wind power density more than 800 w/m2 decline to
the south, 2)the East China Sea area the power density above 400 w/m2 increase to the southward. Guangdong coastal
waters are rich in wind resources energy.
Using ECMWF ERA40 reanalysis, daily rainfall measurements from 740 stations across China, NOAA monthly sea surface temperature (SST) data, NCEP/NCAR monthly outgoing long wave radiation (OLR) data, China NMC-provided daily positions of the western-Pacific subtropical high's ridge, we defined the regional intensity of East-Asian Summer Monsoon (EASM) and calculated the intensity of EASM in the mid-lower Yangtze valley (MLYV) by the definition. The intensity exhibits stronger inter-annual and inter-decadal variability. Analysis is performed of the difference in the circulation, geopotential height and OLR fields between years of strong, weak and normal EASM in MLYV, with preliminary study on the mechanism for key-region SST impacting the monsoon intensity, discovering the intensity in higher positive (negative) correlation with previous winter SST anomalies (SSTA) over the tropical Indian Ocean, waters off East China, and equatorial eastern Pacific (SSTA over waters east of the Philippines), that is, warmer-than-normal SST in the tropical Indian Ocean, and equatorial eastern Pacific and colder-than-normal SST in the east of the Philippines make the western-Pacific subtropical high's ridge southward of mean, its west stretching point westward of normal and intensity higher in comparison to mean, and meanwhile a blocking high is prone to appear around Lake Balkhash, allowing the cold air to move south frequently, therefore, the cold and warm air flows meet in MLYV, converging and rising, leading to the monsoon intensity stronger and the serious floods occur there and vice versa. The findings can serve as an important criterion for the forecasting of the EASM's intensity in MLYY.
Based on 1979-2005 typhoon data and NCEP/DOE AMIP-II reanalysis, a study is performed of behaviors of tropical
cyclones generated in the monsoon trough (MTTC hereinafter) in the western North Pacific as well as effects of the
monsoon trough strength on their production. Evidence suggests that (1) during this period the MTTC yearly number
experiences stages as follows: normal (1979~87), more MTTCs (1988~94), and fewer MTTCs (1995~2005); MTTC
variation is marked by quasi-4 and -2 yearly periods, with 1994 as the change from more to fewer MTTCs in annual
number; (2) in the years of anomalous MTTC number there are great difference in the onset/ending day and genesis
position. In the years of fewer (more) MTTCs in comparison to mean, MTCC starts its activity later (earlier), terminating
on an earlier (later) day, its genesis area is smaller (bigger), located south- (north-) and/or west- (eastward) of mean; 3)
the ITCZ intensity affects the MTTC genesis position and yearly number. When the lower-level western North Pacific
subtropical high is positioned south- (north-) of normal, cross-equatorial flows at Somali and 90~1600E are weaker
(stronger), the monsoon trough is weaker (stronger) with its position south- and/or westward (north- and/or eastward)
with respect to normal. At that time, in the tropopause, the south-Asian high is east- (westward) of mean and the oceanic
upper-air trough is south- and/or westward (north- and/or eastward). And the distribution in the high and lower
troposphere allows the small-value band of vertical wind shear to decrease (increase) for a smaller (bigger) domain for
MTTC genesis, and convection is suppressed (intensified), leading to positive (negative) OLR anomalies over waters
east of the Philippine so that MTTC is generated south- and/or westward (north- and/or eastward) relative to normal and
MTTC annual number is anomalously smaller (greater).
Using daily rainfall measurements from 740 stations across China and European Centre for Medium-Range
Weather Forecasts (ECMWF) upper air reanalysis daily data (1958-2001), we give out climatically characters of East
Asian summer monsoon's (EASM) movement with the definition of the EASM's front, finding out that the transfer of
the rain belt over East China is consistent with the advance and retreat of the EASM. By the EOF (empirical
orthogonal function) analysis of the gridded EASM's index (average for the 28th-45th pentad) from 1958 to 2001 in
area (105°E-150°E,15°N-55°N), it is founded that, the second mode of the EOF analysis exhibits interdecadal
variations and indicate that the movement of EASM has three interdecadal abrupt changes in 1965, 1980 and 1994,
respectively. Therefore, the three interdecadal abrupt changes bring the different processes of the EASM's movement
and lead to the obvious change of the spatial distribution pattern of summer rainfall in East China directly, especially
prior to 1965, the rainfall in the mid-lower reaches of the Yangtze River is much less than normal, while the
precipitation is much more in South China, North China and Northeast China but with decreasing continuously since
1965. However, the rainfall in the mid-lower Yangtze Valley increases continually from 1980, especially from 1994 the
rainfall in South China and the Yangtze Valley increases rapidly while the precipitation over North China was much
less than normal. Therefore, in East China underwent from the pattern of south- drought and northern- waterlog before
1979 to south-waterlog and north- drought.
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