γCas的光谱变化

γ Cas是一颗Be/x-ray双星.紫台于1986年冬用新安装在60cm反光镜上的Marly-Nanjing非球面光(?)摄谱仪对其作了光谱观测.本文简要介绍了观测期间Ha、HeIλ5875与HeIλ6678发射线轮廓的特征及其待值宽度在天与天之间,数小时之间变化.     

模糊马尔科夫过程在地质学中的初步应用

本文主要论述了不严格具有无后效性而与经典马尔科夫过程又有某些类似之处的“模糊马尔科夫过程”,从理论上研究和确定了上述随机过程各个时刻之分布概率及模糊置换分析和模糊熵的计算方法,并介绍了在地质学中的应用实例。结果表明,通过这种方法能够扩大马尔科夫过程的理论研究和应用领域。     

BPM载频产生器的研制

介绍BPM短波投时台新的载频产生器的设计与实现。该BPM载频产生器以原子颁标的5MHz标频信号为参考，利用频率合成技术，产生出供发射机使用的2．5MHz、5MHz、10MHz、15MHz和20MHz五种高准确度的载频信号。这些信号既能单独输出，也可利用面板控制或遥控选择输出。为了保证系统的可靠性，来用了两冗余结构。并设置了必要的报警与指示。     

凡纳滨对虾和斑节对虾对WSSV敏感性的比较

用6.0×104拷贝、1.2×104拷贝和6.0×103拷贝3种剂量白斑综合症病毒(WSSV)对凡纳滨对虾和斑节对虾进行人工注射感染,比较了两种对虾对WSSV敏感性的差异。结果表明,凡纳滨对虾死亡时间随病毒剂量降低而延长,斑节对虾死亡时间没有明显差异;随病毒剂量的降低,凡纳滨对虾人工注射感染后病毒复制高峰时间显著延长,斑节对虾感染后病毒复制高峰时间相同,WSSV在凡纳滨对虾体内比在斑节对虾体内复制慢。对虾携带WSSV数量最低为3.3×107拷贝.g-1,最高为4.3×108拷贝.g-1。凡纳滨对虾比斑节对虾对WSSV的抵抗性更强。     

“这次我竞选所长成功了!”

俗话说:事在人为。这话在张红运身上验证了。第三次参加局举行的中层干部公开竞选活动,这次,张红运经过演讲口试、笔试、民主测评、写作能力等程序后。主持人最后宣布:“按照综合成绩排名先后顺序,张红运等五人任国土资源所所长,试用期一年……”今年初,项城市撤销了城郊、水寨、老城三个乡镇,设立了莲花、东方、水寨、花园、千佛阁、光武六个办事处,基层国土所也随之进行了调整。为做好衔接,项城市国土资源局决定在全系统内公开选拨、调整部分基层所所长。9月22日上午,参加所长职位竞争的19名选手按抽签顺序依次进行。演讲口试、笔试由评委…     

SST variations of the Kuroshio from AVHRR observation

1 INTRODUCTION The Kuroshio Current (KC), being the western boundary current in the North Pacific subtropical gyre, is the second strongest current in the world af- ter the Gulf Stream and is famous as a strong and fast flow. KC plays an important role in…     

沙丘地貌学

沙丘地貌学革命的十年 15年前,Cook 和 Warran(1973)就指出,在荒漠研究方面,通过调查获得资料,然后以大量相互混淆的术语进行肤浅的描述来解释地貌现象仍然是地貌学家的主要手段。     

金龙山地区滑坡研究

金龙山地区位于四川省雅砻江二滩水电站库首左岸。区内海拔1000—2700米;重点研究区海拔<1730米,面积近1.3平方公里。本区滑坡顺层发育,以蠕滑方式为主,成条成群分布,新老俱全,厚度各异(巨厚—表层),规模不一。控制坡体蠕滑和滑动的主要是层面(或似层面)、层间错动带和中缓倾角裂隙。据滑坡活动状况的不同,将全区分为三个滑坡区:Ⅰ区是多级古滑坡区(方量约200万立方米);Ⅱ区是蠕滑区(方量约2000万立方米);Ⅲ区是浅-表层残坡积层滑坡区。     

Deepwater Ventilation and Stratification in the Neogene South China Sea

Combined data of physical property, benthic foraminifera, and stable isotopes from ODP Sites 1148, 1146, and 1143 are used to discuss deep water evolution in the South China Sea (SCS) since the Early Miocene. The results indicate that 3 lithostratigraphic units, respectively corresponding to 21-17 Ma, 15-10 Ma, and 10-5 Ma with positive red parameter (a*) marking the red brown sediment color represent 3 periods of deep water ventilation. The first 2 periods show a closer link to contemporary production of the Antarctic Bottom Water (AABW) and Northern Component Water (NCW), indicating a free connection of deep waters between the SCS and the open ocean before 10 Ma. After 10 Ma, red parameter dropped but stayed higher than the modern value (a*=0), the CaCO3 percentage difference between Site 1148 from a lower deepwater setting and Site 1146 from an upper deepwater setting enlarged significantly, and benthic species which prefer oxygen-rich bottom conditions dramatically decreased. Coupled with a major negative excursion of benthic δ13C at ~10 Ma, these parameters may denote a weakening in the control of the SCS deep water by the open ocean. Probably they mark the birth of a local deep water due to shallow waterways or rise of sill depths during the course of sea basin closing from south to east by the west-moving Philippine Arc after the end of SCS seafloor spreading at 16-15 Ma. However, it took another 5 Ma before the dissolved oxygen approached close to the modern level. Although the oxygen level continued to stabilize, several Pacific Bottom Water (PBW) and Pacific Deep Water (PDW) marker species rapidly increased since ~6 Ma, followed by a dramatic escalation in planktonic fragmentation which indicates high dissolution especially after ~5 Ma. The period of 5-3 Ma saw the strongest stratified deepwater in the then SCS, as indicated by up to 40% CaCO3 difference between Sites 1148 and 1146. Apart from a strengthening PDW as a result of global cooling and ice cap buildup on northern high latitudes, a deepening sea basin due to stronger subduction eastward may also have triggered the influx of more corrosive waters from the deep western Pacific. Since 3 Ma, the evolution of the SCS deep water entered a modern phase, as characterized by relative stable 10% CaCO3 difference between the two sites and increase in infaunal benthic species which prefer a low oxygenated environment. Thesubsequent reduction of PBW and PDW marker species at about 1.2 Ma and 0.9 Ma and another significant negative excursion of benthic δ13C to a Neogene minimum at ~0.9 Ma together convey a clear message that the PBW largely disappeared and the PDW considerably weakened in the Mid-Pleistocene SCS. Therefore, the true modern mode SCS deep water started to form only during the "Mid-Pleistocene climatic transition" probably due to the rise of sill depths under the Bashi Strait.