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marine biota
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  海洋生物群
     A PHASIC ALTERNATION OF MARINE BIOTA FROM LATE ORDOVICIAN TO EARLY SILURIAN AND THE GEOLOGICAL AGE OF THE GUANYINQIAO FORMATION
     扬子区晚奥陶世到早志留世海洋生物群的阶段性更替及观音桥组的时代
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  “marine biota”译为未确定词的双语例句
     Study on the Numerical Simulation of Radiation Nuclide Mass Field and Radiation Dose for Marine Biota in Daya Bay
     大亚湾放射性物质场数值模拟和海洋生物辐射剂量的研究
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     After the operation of GNPS and LNPS, the major source of radioactive nuclide pollution comes from low radioactive polluted water,, The major objective of this paper was to study the diffuse e rule of radioactive nuclide in ocean environment and the impact of radiation dose to marine biota.
     大亚湾核电站(GNPS)和岭澳核电站(LNPS)等运行之后,排入湾内海域的低放射性废液成为放射性污染的主要来源。 本文是对放射性核素液态排放在海洋生态转移、扩散规律以及对海洋生物所致辐射剂量的研究。
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     Dimethylsulfide(DMS),the most important volatile sulfur compound in the oceans,is the main source of sulfur to the atmosphere and plays a key role in the interaction between marine biota and global climate change via the formation of atmospheric aerosol and cloud condensation nuclei.
     DMS是海洋中最主要的挥发性有机硫化物,对全球气候变化和环境酸化产生重要影响。
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  相似匹配句对
     Marine Adhesives
     海洋天然胶粘剂
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     Marine Toxins
     海洋生物毒素
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     ON THE HUAINAN BIOTA
     论淮南生物群
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     Sinian Biota in China
     中国“震旦生物群”
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     A PHASIC ALTERNATION OF MARINE BIOTA FROM LATE ORDOVICIAN TO EARLY SILURIAN AND THE GEOLOGICAL AGE OF THE GUANYINQIAO FORMATION
     扬子区晚奥陶世到早志留世海洋生物群的阶段性更替及观音桥组的时代
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  marine biota
Effect of coastal-protection structures of the Kansai International Airport on functioning of marine biota
      
The admissable contents of technogenic radionuclides, which ensure the safety of the population and marine biota, in the marine waters of the Russian Federation are estimated, 3 tables, 23 references.
      
If biological variables (scavenging rates, primary productivity) remain constant while anthropogenically-derived Hg deposition increases, it is likely that concentrations in marine biota (including fish) will rise in accord.
      
Heavy metal contamination of the marine biota along the Rio de Janeiro coast, SE-Brazil
      
The measurements revealed the importance of nitrous and nitric acids for the transport of nitrogen to marine biota in busy ship lanes.
      
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The palaeobiocoenosis extinction on more than 30 stratigraphic profiles in the Yangzi area was counted. The result shows that the marine biota from late Ordovician to early Silurian has a series of phasic alternation. The general feature of the alternation is as follows:

对扬子区30多个剖面中的古生物绝灭情况进行了统计,结果表明,晚奥陶世到早志留世海洋生物群进行了一系列阶段性更替,更替的总体特征是:(1) 每一个时期生物绝灭后都存在一个复苏期,然后又爆发式地大发展,且发展的生物基本上不再重复已绝灭的生物,而是向更高一级演化;(2) 不同生物的绝灭期和复苏期相互交叉。这种阶段性更替的主要原因是:(1) 奥陶纪末期大规模海退使扬子海处于半封闭状态,这种还原环境的特点是水流不畅,缺氧,食物链被破坏,使底栖生物大批死亡;(2) 奥陶纪末期的大冰期使世界气候普遍变冷,从而促使生物绝灭。这种阶段性更替在五峰期和观音桥期之交表现得更为清楚,规模也更大。从观音桥组的分布特征、岩性特征、形成环境特征及古生物绝灭事件等方面综合分析,认为观音桥组划在志留系底部更为适宜。

Part of the Himalayas which lies between the Tibetan Plateau and theIndian Subcontinent belongs to the eastern part of the Tethyan Tectonic Realm,from where many data had been collected during the last decade (Zhang, 1981;Wan, 1987). It is generally acceptable that the Tibetan Plateau is composed ofdifferent continental blocks which were detached from Gondwana at differentgeological times. 1. Cretaceous Since the beginning of the Cretaceous, the so-called Himalayan Sea wassandwiched between the Indian and Eurasian...

Part of the Himalayas which lies between the Tibetan Plateau and theIndian Subcontinent belongs to the eastern part of the Tethyan Tectonic Realm,from where many data had been collected during the last decade (Zhang, 1981;Wan, 1987). It is generally acceptable that the Tibetan Plateau is composed ofdifferent continental blocks which were detached from Gondwana at differentgeological times. 1. Cretaceous Since the beginning of the Cretaceous, the so-called Himalayan Sea wassandwiched between the Indian and Eurasian plates. In the Early Cretaceous(140--100 m.y.B.P.) a deep sea trough extended along the Indus-Yarlun Zangbo(Tsangpo) belt where ophiolites and deep sea silicolites were deposited. TheHimalayan region extending toward the south of the deep trough was then acontinental slope on the north edge of the Indian Plate. The fact that the seawas rather deep is attested by its rare fauna of ammonoids, bivalves and algaein the black shale deposits of great thickness in this region. After the Mid- Cretaceous, the Yarlun Zangbo Trough ceased its sea-floor spreading and en-tered into its closing episoder this is evidenced by the great thickness of flyschdeposits resulted from the encroachment of the Indian Plate upon the EurasianPlate. The Himalayan region became a continental shelf on the northern edgeof the Indian Plate, due to the general elevation of the region. A prolific faunaof ammonoids, bivalves, both planktonic and benthonic foraminifera lived inthis suitable marine environment with deposits of siltstones, mudstones andlimestones. The sea still further shallowed in the latest Cretaceous (Maastrich-tian).Almost all of the planktons disappeared at this time, whereas the largerbenthonic foraminifera Orbitoidae as well as rudistid and inoceramid bivalvesflourished. A widespread regression occurred in the Himalayan Sea at about the endof the Cretaceous. The sea entered into its last evolutionary phase and graduallywithdrew from the area during the regression, although two transgressions wereinvolved in the Paleocene and Early Eocene. 2. Latest Cretaceous to earliest Paleocene regression During the Late Cretaceous, an oceanic environment existed in the Himala-yan region, which connected with the western Tethys and the Indo-PacificOcean, yielding a community of the Globotruncana, Orbitoides and Omphalocyclusfaunas (Wan, 1985; 1987). In the mid-Maastrichtian to early Danian interval,this region is characterized by marine oscillations, with a regression marked bythe deposition of arenaceous facies of varying thickness over the entire region.The age of the sandstones in different areas suggests that the end-Cretaceousregression proceeded from both east and west towards the Gamba--Tingri region.This regression was brought about by the tectonic events which led to the colli-sion of the Indian Plate with the Eurasian Plate, causing a general elevationalong the northern margin of the Indian Plate. The consequent elevation wasevidenced by the formation of both arms of the Himalayan Sea (Fig. 1). TheLower Indus and Baluchistan Basins in the west and the Assam Basin inthe east became shallower during the Middle Maastrichtian; abundant terrestialmaterial emptied into the basins, and the marine biota became restricted indiversity. Following the elevation of the Lower Indus and Baluchistan Basins,the Upper Indus Basin was influenced by the regression in the Late Maastrich-tian. The reaction to the elevation in the Zhongba Basin was even later, wherethe regression phase spanned the Latest Maastrichtian and Early Danian. Theregression did not reach the Gamba-Tingri Basin until the Early Danian, whenit gave rise to the deposition of the Jidula Sandstone. 3. Paleocene After the end-Cretaceous regression, deep water environments ceased to existin the Himalayan Sea. This regression phase was followed by the Paleocenetransgression, producing a continental shelf environment connecting the Indianand Eurasian plates and extending into a narrow belt from the Gamba-TingriBasin westwards to Pakistan and eastwards to Assam along the Himalayas. The e

由于印度板块向北漂移,使特提斯-喜马拉雅海在白垩纪后期进入了衰退时期.在白垩纪—第三纪的不同阶段中,陆壳的升降运动造成了海平面的变化,形成了不同的生态环境。本文主要依据不同时期不同地区的有孔虫化石组合特征,分析了特提斯-喜马拉雅海在白垩纪至早第三纪的演变过程,揭开了青藏高原隆升的序幕。

The Dingjiazhai Fm. aged Asselian-Sakmarian pseudoconformably overlles the Pumenqian Fm. aged the Lower Carboniferous. The Dingjiazhai Fm. in the Dingjiazhai section at Shidian County mainly comprises 3 parts in ascending order: 1. the pebble-bearing layer at the lower part; 2. siltstones and black shales at the middle part in which trace fossils PalaeoPhycus sp., Taenidium serpentinum, have been found, 3. muddy siltstones and biocalcarenites at the upper part. A thin purple mudstone occurs at its topmost in...

The Dingjiazhai Fm. aged Asselian-Sakmarian pseudoconformably overlles the Pumenqian Fm. aged the Lower Carboniferous. The Dingjiazhai Fm. in the Dingjiazhai section at Shidian County mainly comprises 3 parts in ascending order: 1. the pebble-bearing layer at the lower part; 2. siltstones and black shales at the middle part in which trace fossils PalaeoPhycus sp., Taenidium serpentinum, have been found, 3. muddy siltstones and biocalcarenites at the upper part. A thin purple mudstone occurs at its topmost in which the trace fossil Dendrotichnium sp., is present. According to the palaeontological, petrological and ichnological features, six main sedimentological facies are distinguished from the upper part of Pumenqian Fm. to the Dingjiazhai Fm. They are tidal flat facies, margin facies and lagoon facies which were located in the restricted platform,sand bar or shoal facies, basin facies of shallow water and open marine platform which belonged to open marine environments. The Dingjiazhai Fm. in the Jinji section of Baoshan region consists of the pebble-bearing layer at its lower part and mudstones and muddy siltstones at its middle and upper part. Palaeo phycus sp. B and Tisou jinjiensis are main trace fossils present in the mudstones and muddy siltstones overlying the pebble-bearing layer. The vertical U-shaped structures of Tisoa jopnsis are similar to those of Areni colites. The trace fossil assemblage can be attributed to the Skolithos ichnofacies. As indicated by Frey & Pemberton (1984), the environtnents which the Skolithos ichnofacies represents are characterized by shifting substrates, moderate to high-energy conditions and episodic erosion or deposition. On the basis of petrological studies on the pebble-bearing layer, it can be divided into two beds: the lower pebble bed and the upper brecciated limestone. The pebbles with better rounding in the former are elliptical and flat and mainly consist ofsiltstones, quartzites, silicolltes and lithic sandstones. The breccia in the latter are briefly composed of llmestones whose carbonate microfacies are similar to those of the underlying Pumenqian Ftn..The cementation of the brecciated limestone is much better than that of the lower pebble bed. The authors consider that the origin of the pebble-bearing layer at the lower part of the Dingjiazhai Fm. is not related to glaciation. The Iower pebble bed was deposited in the normal littoral environments and the upper brecciated llmestone was derived from the debris flow. The palaeoecologic features of biota (corals, fusulinids, spores) also indicate that the organisms lived in warm marine environments. Many geologists have regarded striated clasts, dropstones,three-fold sequence and periglacial marine biota as main evidences of glacial origin of the Dingjiazhai Fm.This paper puts forward different viewpoints against thelr conclusions. The striated clasts are not only products of glacial process. They can be produced by many other geological processes such as faults, debris flow,landslip, landfall, mountain flood and even wind action. The photos of striated clasts (Fan & Fang, 1992) do not show any typical characters generated by glaciatlon. They have better roundness and lack evident worn planes. The direction of striates is different from that of long axis of clastsSome Chinese and foreign geologists misunderstand that the dropstones are able to stab the stratification when they fall down. In fact, when the dropstones fall down and come into contact with the surface of deposits, the power of dropstones is not strong enough to crash the stratification and only can bend it. The local concentration of pebbles and coarse clasts and the occurrence of tin Pellets can be regarded as products of iceberg raft. Un fortunately, these phenomena have not been found in the Dingjiazhai Fm.Wopfner (1994) suggest that the three-fold sequence consisting of 1. diamictites and coarse clasticsl 2. pebbly mudstones and laminites and 3.black pyritic mudstones respectively correspond to the deposits in glacial advance, glacial retreat and deglacia

丁家寨组的沉积特征表明,自二叠纪初阿赛尔期至萨克马尔期在云南保山地区为一持续的海进过程,其下都含砾层可分成两种成因类型:滨海相成因的下部砾岩层和碎屑流成因的上部角砾状灰岩层。文章就了家寨组在横向上的展布特点和纵向上岩相变化规律以及其中所含的海相化石等,对含砾层的各种冰川成因说提出了质疑,并用翔实的资料对区内冰川成因说的重要证据(条痕石、落石、三重序列、冰绿海生物群)提出否定意见。

 
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