2004年4月11日AR0588中环形暗条爆发与CME的研究

利用云南天文台色球Hα单色像、SOHO/EITEUV单色像、SOHO/LASCO白光日冕观测、SOHO/MDI光球磁图及Nobeyama17GHz微波射电观测资料对2004年4月11日AR0588中的环形暗条爆发进行了初步的分析。主要结论如下:(1)爆发的暗条呈现封闭的环形。在Hα观测上爆发前有明显的激活态,表现为西半环变粗变厚,断裂出现缺口并缓慢向西南方向上升。在EIT195 观测上,此暗条爆发表现出两条扎根于爆发源区的亮带,其顶部可能是爆发中的暗条,而这两条亮带是暗条的两条腿。该暗条爆发是动力学爆发,但暗条等离子体在爆发过程中也受到明显的加热。(2)该暗条爆发伴随有一个明显的双带耀斑。一个带位于暗条爆发的中心,几乎不动,而另一个带呈环状包围爆发的暗条,展示明显的分离运动。这两个带之间,在耀斑后期出现明显的耀斑后环。(3)这一暗条爆发及耀斑与LASCO观测到的一个快速的、具有典型三部分结构的partialHaloCME在时间和空间上是密切相关的。     

基于MDI/SOHO合成图的全球磁场外推

用势场方法和格林函数解构造了三维日冕磁场.相关的边界条件是所观测的光球磁场以及光球上2.6个太阳半径的开放场(源表面).所用的光球数据来自高精度的MDI/SOHO观测(2″/像素,1桢/98min).这种外推方法可以用来分析太阳大事件在大尺度上的可能触发机制.作为一个例子,我们分析了活动区NOAA9077的外推日冕场,发现它们的形态与EIT/SOHO的日冕观测相符很好.结合全日面Hα演化,我们推测来自活动区9082的一次激波扰动应该是导致2000年7月14日大耀斑和日冕物质抛射的触发原因,该扰动沿着外推所得到的一个磁环系统直接传到大耀斑爆发位置.     

基于MDI／SOHO合成图的全球磁场外推

用势场方法和格林函数解构造了三维日冕磁场，相关的边界条件是所观测的光球磁场以及光球上2.6个太阳半径的开放场（源表面），所用的光球数据来自高精度的MDI/SOHO观测（2″/像素，1桢/98min），这种外推方法可以用来分析太阳大事件在大尺度上的可能触发机制，作为一个例子，我们分析了活动区NOAA9077的外推日冕场，发现它们的形态与EIT/SOHO的日冕观测相符很好，结合全日面Ha演化，我们推测来自活动区9082的一次激波扰动应该是导致2000年7月14日大耀斑和日冕物质抛射的触发原因，该扰动沿着外推所得到的一个磁环系统直接传到大耀斑爆发位置。     

2003年8月太阳活动区AR0442内的暗条爆发及其相关现象的研究

利用色球Ha单色像、TRACE和SOHO／EITEUV单色像、SOH0／LASCO白光日冕观测及SOH0／MDI光球磁图，对2003年8月25日日面AR0442边界上2个暗条爆发的不同动力学行为及与之相关的耀斑、耀斑后环和CME等现象进行了分析。主要结论如下：(1)2个暗条的激活态和爆发过程有明显不同：暗条F1先变粗变黑，出现明显分叉，然后表现为whiplike爆发；而暗条F2一部分先消失，其余部分出现水平的轴向运动，最后F2整体爆发。(2)2个暗条的爆发机制是不同的：F1的爆发可能与新浮磁流密切相关，而F2的爆发与F1爆发产生的双带耀斑的分离运动和相互作用密切相关。     

耀斑前兆相日冕环的色球足点增亮和兰移

报导了云南天文台精细结构望远镜观测到的耀斑前兆相的日冕环的色球足点增亮和兰移现象。两个日冕环的４ 个足点由 Ｙｏｈｋｏｈ／ Ｈ Ｘ Ｈ／ Ｓ Ｘ Ｔ 的观测研究所确认。在耀斑前, 色球上与日冕环足点相对应的、分立的点状亮谱斑,其偏带观测显示出兰移, 表明它们是日冕环的色球足点, 且表明存在着物质的预加热, 以及物质从足点沿冕环向上流动。观测还显示冕环所跨越的暗条的激活。这些现象清楚说明, 物质沿磁力线的“蒸发”发生在耀斑前兆相, 而且,色球磁场的剧烈变化可能是引起色球蒸发的原因之一     

1988年3月黑子磁场的演化(英文)

024黑子(S.G.D编号为4964)是1988年3月份太阳上最大、磁场最强的黑子群。在日面上出现的半个月里,始终有耀斑产生。北京天文台怀柔太阳磁场望远镜对这个活动区作了常规观测,并获得了磁场和速度场资料。 024活动区是由一个偶极黑子和δ黑子组成的。12日01~h49~mUT,黑子刚从东部出现时就有耀斑和活动日珥产生。从速度场与H_β色球单色像对比来看,耀斑内有物质向里流动,而暗条中有物质向外抛射。024活动区的磁场十分复杂,S极、N极磁场互相包含、渗入、剪切,形成许多海湾结构。可能这就是产生了许多各种形状的耀斑的缘故。本文对磁场的形态作了描述。     

1981年4月1日日面4N耀斑环系的光学前兆与活动特征

根据云南天文台太阳色球H_α和相应的光球黑子观测以及磁场测量,并结合有关X—ray资料等,对1981年4月1日日面4N大耀斑进行了部份测量和分析。结果表明,该耀斑为环系;光球浮现磁流和黑子扭曲、挤压和剪切运动是触发该耀斑的直接原因。而活动的黑子光桥又是浮现磁流的一种重要标志;耀斑环或带与磁场位形密切相关;耀斑后在运动空间原位置处光球又浮现出部份磁流;卵形暗条内预示能爆发大耀斑。     

投影改正后CME的速度分布

目前观测的CME(日冕物质抛射)是其在天空平面的投影,这就导致CME的观测参量与真实参量之间存在一定的差异,比如说观测到的CME速度一般要比CME的真实速度小.运用基于锥状模型对CME的速度进行投影改正的方法,分析1996年9月到2007年9月(将近1个活动周)SOHO/LASCO日冕仪观测到的1 691个仅与耀斑相关的CME(简称FL类CME)和610个仅与暗条爆发相关的CME(简称FE类CME)投影改正前后的速度分布,得到如下结果:(1)投影改正前后,FL类CME和FE类CME的速度分布非常相似.且投影改正前后,两类CME的平均速度几乎相同; (2)投影改正前后,FL类CME和FE类CME速度的自然对数分布也非常相似.     

对2007年5月23日的一个CME的起源和初始阶段的观测研究

利用多波段联合观测数据,综合分析研究了一个发生于2007年5月23日的日冕物质抛射(Coronal Mass Ejection,CME)爆发事件的起源和初始阶段的物理演化过程.该CME起源于活动区10956内的一个并没有严格地位于活动区极性反转线上的U形活动区暗条,该暗条首先被扰动,然后从中间部分开始缓慢上升.在暗条上升运动过程中,从极紫外和软X射线像上可观测到位于暗条上方的日冕磁环也在不断地上升并且有持续向外的扩张运动.最终,这些冕环和暗条一起爆发并伴随着一个位于暗条断开位置附近的日冕暗化区域的形成.这一爆发过程还伴随着一个静止轨道业务卫星(GeostationaryOperational Environmental Satellites,GOES)软X射线流量级别为B5.3的亚耀斑发生,该光斑显示出与CME之间具有在时间和空间上的紧密联系.与CME的"标准"磁流绳模型一致,这些太阳表面活动可以看作是CME的初始演化阶段在日面上的表现信号,并且该CME的亮前锋可能是由预先存在于暗条上方的冕环体系直接演化而来.另外,文中还讨论了与该事件相关的暗条爆发、耀斑、冕环扩张和消失以及日冕暗化之间的关系.     

晕状日冕物质抛射

主要介绍晕状日冕物质抛射（halo CMEs)的产生机制，包括向量磁场演化是怎样触发halo CMEa的：halo CME与耀斑，暗条活动的相互关系怎样，是否有规律可循，暗条爆发，耀斑等活动现象是如何相互联系的，halo CME事件是由一个活动区域或一个活动事件驱动物，还是多个活动区或多个活动事件相互作用的结果，给出两个halo CME的日面起源的观测例证，提出相反极笥的磁场对消是CME日面源区磁场演化的主要特征。     

Instructions for authors

正Research in Astronomy and Astrophysics publishes original research papers and reviews 011 all liranchcs of astronoiriy and astrophysics.Reviews arc by invitation only.Important new results that require rapid publication can be submitted as a Letter(Letters must be restricted in length     

A thermodynamic model of high temperature lava vaporization on Io

We modified the MAGMA chemical equilibrium code developed by Fegley and Cameron (1987, Earth Planet. Sci. Lett. 82, 207-222) and used it to model vaporization of high temperature silicate lavas on Io. The MAGMA code computes chemical equilibria in a melt, between melt and its equilibrium vapor, and in the gas phase. The good agreement of MAGMA code results with experimental data and with other computer codes is demonstrated. The temperature-dependent pressure and composition of vapor in equilibrium with lava is calculated from 1700 to 2400 K for 109 different silicate lavas in the ONaKFeSiMgCaAlTi system. Results for five lavas (tholeiitic basalt, alkali basalt, Barberton komatiite, dunite, and a molten type B1 Ca, Al-rich inclusion) are discussed in detail. The effects of continuous fractional vaporization on chemistry of these lavas and their equilibrium vapor are presented. The predicted abundances (relative to Na) of K, Fe, Si, Al, Ca, and Ti in the vapor equilibrated with lavas at 1900 K are lower than published upper limits for Io's atmosphere (which do not include Mg). We predict evaporative loss of alkalis, Fe, and Si during volcanic eruptions. Sodium is more volatile than K, and the Na/K ratio in the gas is decreased by fractional vaporization. This process can match Io's atmospheric Na/K ratio of 10±3 reported by Brown (2001, Icarus 151, 190-195). Silicon monoxide is an abundant species in the vapor above lavas. Spectroscopic searches are recommended for SiO at IR and mm wavelengths. Reactions of metallic vapors with S- and Cl-bearing volcanic gases may form other unusual gases including MgCl₂, MgS, MgCl, FeCl₂, FeS, FeCl, and SiS.     

Instructions for authors

正Research in Astronomy and Astrophysics publishes original research papers and reviews on all branches of astronomy and astrophysics.Reviews are by invitation only.Important new results that require rapid publication can be submitted as a Letter(Letters must be restricted in length to 6 printed pages).Authors who submit a paper are expected to be able to certify that the paper is original work,     

Alkali and halogen chemistry in volcanic gases on Io

We use chemical equilibrium calculations to model the speciation of alkalis and halogens in volcanic gases emitted on Io. The calculations cover wide temperature (500-2000 K) and pressure (10⁻⁶ to 10⁺¹ bars) ranges, which overlap the nominal conditions at Pele (T=1760 K, P=0.01 bars). About 230 compounds of 11 elements (O, S, Li, Na, K, Rb, Cs, F, Cl, Br, I) are considered. The elemental abundances for O, S, Na, K, and Cl are based upon observations. CI chondritic elemental abundances relative to sulfur are used for the other alkalis and halogens (as yet unobserved on Io). We predict the major alkali species in Pele-like volcanic gases and the percentage distribution of each alkali are LiCl (73%), LiF (27%); NaCl (81%), Na (16%), NaF (3%); KCl (91%), K (5%), KF (4%); RbCl (93%), Rb (4%), RbF (3%); CsCl (92%), CsF (6%), Cs (2%). Likewise the major halogen species and the percentage distribution of each halogen are NaF (88%), KF (10%), LiF (2%); NaCl (89%), KCl (11%); NaBr (89%), KBr (10%), Br (1%); NaI (61%), I (30%), KI (9%). We predict the major halogen condensates and their condensation temperatures at P=0.01 bar are NaF (1115 K), LiF (970 K); NaCl (1050 K), KCl (950 K); KBr (750 K), RbBr (730 K), CsBr (645 K); and solid I₂ (200 K). We also model disequilibrium chemistry of the alkalis and halogens in the volcanic plume. Based on this work and our prior modeling for Na, K, and Cl in a volcanic plume, we predict the major loss processes for the alkali halide gases are photolysis and/or condensation onto grains. Their estimated photochemical lifetimes range from a few minutes for alkali iodides to a few hours for alkali fluorides. Condensation is apparently the only loss process for elemental iodine. On the basis of elemental abundances and photochemical lifetimes, we recommend searching for gaseous KCl, NaF, LiF, LiCl, RbF, RbCl, CsF, and CsCl around volcanic vents during eruptions. Based on abundance considerations and observations of brown dwarfs we also recommend a search of Io's extended atmosphere and the Io plasma torus for neutral and ionized Li, Cs, Rb, and F.     

The climatic and physiographic controls of the eastern Mediterranean over the late Pleistocene climates in the southern Levant and its neighboring deserts

Modern-day synoptic-scale eastern Mediterranean climatology provides a useful context to synthesize the diverse late Pleistocene (60–12 ka) paleohydrologic and paleoenvironmental indicators of past climatic conditions in the Levant and the deserts to its south and east. We first critically evaluate, extract, and summarize paleoenvironmental and paleohydrologic records. Then, we propose a framework of eastern Mediterranean atmospheric circulation features interacting with the morphology and location of the southeast Mediterranean coast. Together they strongly control the spatial distribution of rainfall and wind pattern. This cyclone–physiography interaction enforces the observed rainfall patterns by hampering rainfall generation south and southeast of the latitude of the north Sinai coast, currently at 31°15′.The proposed framework explains the much-increased rains in Lebanon and northern Israel and Jordan as deduced from pollen, rise and maintenance of Lake Lisan, and speleothem formation in areas currently arid and semiarid. The proposed framework also accounts for the southward and eastward transition into semiarid, arid, and hyperarid deserts as expressed in thick loess accumulation at the deserts' margins, dune migration from west to east in the Sinai and the western Negev, and the formation of hyperarid (< 80 mm yr^− 1) gypsic–salic soils in the southern Negev and Sinai. Our climatic synthesis explains the hyperarid condition in the southern Negev, located only 200–250 km south of the much-increased rains in the north, probably reflecting a steeper rainfall gradient than the present-day gradient from the wetter Levant into its bordering southern and eastern deserts.At present, the rainiest winter seasons in Lebanon and northern and central Israel are associated with more frequent (+ 20%), deeper Cyprus Lows traversing the eastern Mediterranean at approximately the latitude of southern Turkey. Even these wettest years in northern Israel do not yield above average annual rainfall amounts in the hyperarid southern Negev. This region is mainly influenced by the Active Red Sea Troughs that produce only localized rains. The eastern Mediterranean Cyprus Lows also produce more dust storms and transport higher amounts of suspended dust to the loess area than any other atmospheric pattern. Concurrent rainfall and dust are essential to the late Pleistocene formation of the elongated thick loess zone along the desert northern margin. Even with existing dust storms, the lack of rain and very sparse vegetation account for the absence of late Pleistocene loess sequences from the southern Negev and the formation of hyperarid soils.When the north Sinai coast shifted 30–70 km northwest due to last glacial global sea level lowering, the newly exposed coastal areas supplied the sand and dust to these active eastern Mediterranean cyclones. This enforced the latitude of the northern boundary of the loess zone to be directly due east of the LGM shoreline. This shift of coast to the northwest inhibited rainfall in the southern Levant deserts and maintained their hyperaridity. Concurrently, frequent deep eastern Mediterranean Cyprus Lows were funneled along the northern Mediterranean increasing (probably doubling) the rains in central and northern Israel, Lebanon, southwestern Syria and northern Jordan. These storms and rains formed lakes, forests, and speleothems only a short distance north of the deserts in the southern Levant.     

Active hot star shells

Interferometry in the visible provides milliarcsecond spatial resolution and thus has been used for studying the circumstellar environment of active hot stars. In this paper I will illustrate how the visibility modulus and phase can be used to better constrain the physics of Be disks through results from the VLA, the MkII and the GI2T interferometers. I will insist on the importance and the potential of coupling high angular resolution with high spectral resolution to the study of Be shells. Finally I will present a possible study of the circumstellar disk of Be stars using the VLTI. This revised version was published online in July 2006 with corrections to the Cover Date.     

Fitting X-ray Afterglow Light curves of Gamma-ray Bursts by Using the Magnetar Energy Injection Model

The central compact object for some gamma-ray bursts (GRBs) may be a strongly magnetized millisecond pulsar. It can inject energy to the outer shock of the GRB by through the magnetic dipole radiation, and therefore causes the shallow decay of the early afterglow. Recently, from a large number of GRB X-ray afterglows observed by Swift/XRT(X-ray telescope), it is revealed that many of them exhibit the shallow decay about 10²∼10⁴ s after the burst prompt emission. We have fitted the X-ray afterglow light curves of 11 GRBs by using the energy injection model of a magnetar with the rotation period in the millisecond order of magnitude. The obtained result shows the validity and universality of the magnetar energy injection model in explaining the shallow decay of afterglows, and simultaneously provides some constraints on the magnetic field strength and rotation period of the central magnetar.     

Natural superrotation of a rarefied planetary atmosphere

We consider the kinetics of a rarefied rotating planetary atmosphere. The spatial distributions of the atmospheric-gas density and mean angular velocity were determined by analyzing the exact solution of the two-dimensional kinetic equation. We show that the angular velocity of the gas at some distance from the planet could be higher than that in the initial layer starting from which the atmosphere is rarefied. Our model calculations elucidate the superrotation mechanism under consideration.