新安江流域上空云内外巨盐核的分布

1979—1980年6—7月份在新安江流域上空进行了云内外巨盐核的观测,得到:(1)大气中云内外的巨盐核浓度分布都与天气背景有关;(2)云内巨盐核浓度大于同高度上的云外巨盐核浓度,不同云内巨盐核浓度和谱型不一样;(3)云内巨盐核浓度要比小云滴少两个量级,因此巨盐核作为凝结核,对形成小云滴的贡献是很小的。     

我国东部巨盐核分布及盐碱土源的初步探讨

从盐核地区分布的观点来看,盐核源地和气象条件对盐核的分布和变化都是很重要的,关于大气盐核与气象条件和海洋源地的关系,过去已有较多研究,而对陆上源地的研究却很少。在我国北方和邻国地面复盖着广阔盐碱土,它如同海面,在风的作用下,将土壤盐粒带入空中大气并扩散传播,从而影响我国东部盐核分布。本文利用我国东部地面和高空巨盐核观测资料,结合地面盐核源地和850hpa气     

我国近海和陆地巨型盐核的分布特点和变化规律

本文介绍了1978年9、10月分别在我国海洋岛、大连和北京的盐核观测结果以及盐核浓度的日变化和日际变化规律等。得出盐核的浓度与湿度、风向风速、低层湿度场以及天气系统等有一定的关系。     

江淮地区大气盐核分布特征的初步分析

一测量大气盐核对研究暖云降水有着十分重要的意义。1980年6—7月我们在安徽省利用人工降雨飞机进行了大气盐核的观测,初步得出了江淮地区大气盐核的浓度、大小及其垂直、水平分布上的一些特征。本文盐核资料均是利用飞机云滴取样器取样、由斑点法进行盐核的检测而得来的。     

江苏地区二氧化碳浓度时空分布特征分析

利用瓦里关和上甸子大气本底站观测的月平均CO₂浓度数据对GOSAT卫星反演的CO₂浓度数据进行验证,结果表明GOSAT产品与台站观测数据有较好的一致性.利用2009年6月—2011年5月GOSAT反演的CO₂浓度数据,分析了江苏地区CO₂浓度的时空变化特征,结果表明:1)975 hPa高度层CO₂浓度高于850 hPa高度层,CO₂浓度的水平变化要小于垂直变化;2)在季节变化上,CO₂浓度冬季最高,夏季最低,这可能与植被光合作用的强弱变化有关;比较前后两年的CO₂浓度数据,夏季和秋季的增速较快,冬季和春季的增速较慢;3)在日变化上,发现徐州和南京站02时CO₂浓度最高,14时CO₂浓度最低,这可能也与植被光合作用的强弱有关.     

南京大厂地区二氧化硫浓度的常年分布

本文利用作者修正的大气扩散模式,计算了南京市大厂地区SO_2度的常年分布,为城镇总体规划提供了一定的依据;同时表明,此法要比仅用气候资料如风频、污染系数等进行总体规划有更大的优越性。     

黑河地区沙漠气溶胶浓度和谱分布特征

本根据黑河地区的观测结果．着重分析了沙漠气溶胶浓度及其谱分布特征。沙漠气溶胶浓度较低，其中细粒子占绝对优势。扬尘时气溶胶浓度显增加，其中粗粒子增加幅度最大．比平时高20倍以上．直径(D）在2.0-10．0μm间的粗粒子浓度比重从晴天的1.9％上升到9．6％。中等降雨对D>4．0μm的沙漠气溶胶粒子的清除效率非常高(>90％)，但对总浓度的清除效果不很明显(42．5％)，尤其是对其中的D<0．4μm的小粒子(32．8％)，因此0．5相似文献   

广州盛夏期海盐核(Cl~-)巨粒子的分布特征

本文分析了1987年8至9月间在广州观测的Cl~-巨盐核资料。主要结果有:①干直径大于2μm的Cl~-核平均浓度31个/L,平均含盐量0.84μg /m~3,其中于直径大于4μm的特大核平均为3个/L,最大于直径25μm,均远低于南海海域的值。②浓度谱呈典型的单峰型幂函数递减谱,谱型窄而光滑;质量谱也表现为单峰分布。③盐核的日际变化与天气系统有密切关系,台风活动可造成海盐粒子浓度的大量增多,形成所谓“盐核暴”现象。     

尿素核和盐核的凝结性能

尿素作为人工降水暖云催化剂,已有一些地区进行过外场作业和试验.但是关于尿素核的凝结性能,详细的研究甚少.本文对尿素核的凝结增长性能进行了实验研究.作为比较,对常用的暖云催化剂盐核的凝结性能也作了相应的研究.     

北京地区1963年春季冰核浓度变化特点的观测分析

1963年3月18日至4月30日在北京利用混合型云室进行了-15℃至-30℃温度范围内冰核浓度的测定。得到了在4个温度下(-15°,-20°,-25°,-30℃)的平均冰核浓度和冰核浓度的逐日变化的观测结果。 当能见度变低和测点处于市区的下风方向时,观测到的冰核浓度显然较高,这表示城市污染是造成北京地区冰核浓度逐日变动的一个重要原因。另外,在有风砂现象时也常观测到冰核浓度的相对增加,看来北京地区的土壤可能是冰核的另一个比较次要的来源。     

我国东部(30°N)从海岛到陆地巨盐核观测

1983年5月和8月在普陀(海岛)、宁波(沿海)和建德(内陆)三地同时进行了巨盐核的定时观测,取到样品1420份。三测站都位于纬度30°N左右,普陀到建德相距约300公里。观测结果表明:巨盐核主要来自海上;巨盐核浓度与天气背景、风向风速和潮汐现象等有关。并且还讨论了巨盐核浓度的大小分布、日变化规律以及巨盐核的水平输送等问题。     

Measurements of natural ice nuclei with a continuous flow diffusion chamber

Measurements of natural ice nuclei were made in winter continental airmasses with a continuous flow thermal gradient diffusion chamber (described in a separate paper). Over the range of temperatures −7°C to −20°C, the concentration of ice nuclei was closely related to ice supersaturation (SS_i) for humidities both below and above water saturation. Measurements below water saturation were interpreted as deposition nuclei with average concentrations (per liter) approximately 0.32 SS_i(%)^0.81. Measurements were made up to 5% above water saturation and activated both deposition and condensation-freezing nuclei. The average concentration of condensation-freezing nuclei was 0.25 e^{−0.15 T(°C)}. Sample residence time in the chamber was probably too small to detect contact nuclei, unless the nucleating aerosols are extremely small. There was large variability in nucleus concentrations, as much as two orders of magnitude at −15°C. Comparisons are made between these ice nuclei measurements and aircraft observations of ice crystal concentrations in winter orographic clouds.     

西太平洋热带海域海盐粒子的观测和结果

1986年10月15日至12月15日西太平洋热带海域(6°30′N__5°00′S,127°00′__150°00′E)182份海盐粒子资料分析结果:该海域海盐粒子总平均数浓度为107个/l,总平均质量浓度为2.O×10~(-10)g/l,表明该海域可能是海盐粒子低产区;盐粒子浓度与风速有正相关趋势。小风速时的高粒子浓度可能是海盐粒子的1_2天滞留时间所致,也可能是经过本站的气团属性和经历不同造成的;海面流场对盐粒子浓度大小也有一定影响。     

On the relative role of sea salt cloud condensation nuclei (CCN)

Contrasts between cloud condensation nuclei (CCN) spectral volatility (thermal fractionation) measurements in two aircraft field projects provide insight into the relative contribution of sea salt. During the much more cloudy Rain in Cumulus over the Ocean (RICO) project there was a high correlation coefficient (R) between refractory (non-volatile) CCN concentrations (N_CCN) and horizontal wind speed (U), especially for low supersaturation (S) N_CCN, whereas this R was significantly lower in the nearly cloud free Pacific Aerosol Sulfur Experiment (PASE) project. Volatile N_CCN at all S were uncorrelated with U. Ambient particle concentrations over a broad range of large sizes displayed consistently high R with U in both projects that was similar to the R of refractory N_CCN with U in RICO. The size range of this high R extended down to 0.2 μm in RICO but only down to 9 μm in PASE. In both projects particle concentrations smaller than these respective sizes were highly correlated with N_CCN, at all S in PASE, but mainly with N_CCN at high S in RICO. In each project N_CCN at all S was uncorrelated with all ambient particle concentrations larger than these same respective sizes. N_CCN at all S was also uncorrelated with U in both projects. The contrast in cloudiness between the two projects was responsible for many of the differences noted between the two projects. The results indicate that the effects of clouds on N_CCN play a major role in the relative influence of sea salt on N_CCN and ultimately on climate. Sea salt is a minor component of maritime CCN except at high wind speeds especially at low S.     

Measurements of spray at an air-water interface

The spray content in the surface boundary layer above an air—water interface was determined by a series of measurements at various feteches and wind speeds in a laboratory facility. The droplet flux density N(z) can be described in terms of the scaling flux density N_* and von Karman constant K throguh the equation, N(z)/N_* = −(1/K) ln(z/z_0d) where z is height above the mean water level and z_0d is the droplet boundary layer thickness. N_* is given by a unique relationship in terms of the roughness Reynolds number u_*σ/ν where σ is the root-mean-square surface displacement. Spray inception occurred for u_* 0.3. The dominant mode of spray generation in the present and most other laboratory tests, as well as in available field data, appears to be bubble bursting.     

On Measurements of the Tide at Churchill,Hudson Bay

Since the late 1990s the semi-diurnal tide at Churchill, on the western shore of Hudson Bay, has been decreasing in amplitude, with M₂ amplitudes falling from approximately 154?cm in 1998 to 146?cm in 2012 and 142?cm in 2014. There has been a corresponding small increase in phase lag. Mean low water, decreasing throughout most of the twentieth century, has levelled off. Although the tidal changes could reflect merely a malfunctioning tide gauge, the fact that there are no other measurements in the region and the possibility that the tide is revealing important environmental changes calls for serious investigation. Satellite altimeter measurements of the tide in Hudson Bay are complicated by the seasonal ice cover; at most locations less than 40% of satellite passes return valid ocean heights and even those can be impacted by errors from sea ice. Because the combined TOPEX/Poseidon, Jason-1, and Jason-2 time series is more than 23 years long, it is now possible to obtain sufficient data at crossover locations near Churchill to search for tidal changes. The satellites sense no changes in M₂ that are comparable to the changes seen at the Churchill gauge. The changes appear to be localized to the harbour, or to the Churchill River, or to the gauge itself.     

Concentration and size variation of condensation nuclei at Mawson,Antarctica

Condensation nucleus (CN) concentrations have been measured at Mawson (67.6°S, 62.9°E) since mid 1981. Weekly median concentrations have an annual cycle with a maximum of around 300 to 400 cm^-3 in summer and a minimum of a few tens of particles per cm^-3 in winter. In this respect Mawson behaves very much like an Antarctic continental location. Preliminary measurements of the size distribution of CN particles taken over a nine month period suggest a seasonal change in typical particle radius from around 0.01 m in winter to around 0.04 m in summer. Diurnal variation in the CN concentration is generally very weak and does not show any systematic relation to the pronounced diurnal variation in wind-speed at Mawson.Department of Science, Antarctic Division