The Late Cenozoic Diatoms of Sites 183193, Leg 19 Deep Sea Drilling Project
The Late Cenozoic Diatoms of Sites 183193, Leg 19 Deep Sea Drilling Project
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183193号地点的晚新生代硅藻，第19段深海钻探项目
DOI：
10.2973/dsdp.proc.19.130.1973
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发表时间：
1973
期刊：
影响因子：
1.6
通讯作者：
I. Koizumi
中科院分区：
文献类型：
--
作者：
I. Koizumi
北太平洋海底的一大片区域被含有硅藻、硅鞭毛藻和放射虫等微化石的硅质沉积物所占据（Lisitsyn 1971）。这些硅质沉积物主要由硅藻阀，无定形的生物二氧化硅组成，除了赤道以北，北纬10°左右的放射虫软泥区（Riedel, 1959）。Jouse et al.（1969,1971）总结了太平洋单位重量表层沉积物中硅藻瓣的数量分布。由于缺乏良好的碳酸盐组分，北太平洋岩心在硅质微化石领域，特别是硅藻微化石领域进行了微古生物学研究。关于北太平洋深海岩心硅藻地层的第一份报告是由Kolbe（1954）完成的。他指出，由瑞典深海考察队从太平洋赤道部分采集的76号岩芯的较低层次上存在第三纪物种，岩芯的下部和上部之间存在明显的差异。自科尔贝以来，苏联的一些工作者对北太平洋及其邻近海域的深海岩心中的硅藻进行了非常积极的研究；即白令海、鄂霍次克海和日本海。通过系统的研究，俄罗斯工作者确信（如Jouse， 196Id, 1962）：(a)海底沉积物最上层的硅藻藻群落在很大程度上取决于上面水团中的生物群落，(b)物种组成反映了上覆水团的海洋学条件，(c)海底沉积物中硅藻组合的地理地带性很好地表现在它们目前在太平洋的分布中。(d)第四纪期间的气候变化引起海洋生物地理带的位移，与上层水团的位移同步，因此(e)可以从硅藻种类组成的变化来判断沉积物积聚期间的热条件（Jouse 196Id）。关于深海岩心硅藻地层的报告如下：Seczkina（1959）关于日本海长岩心中的硅藻；jous<e:1> (1961a, b)，关于太平洋西北部长岩心中以硅藻为标志的层位的对比；Jouse(1962)，对俄罗斯工人在苏联远东海域（白令海、鄂霍次克海、日本海和北太平洋西北部）进行的硅藻研究的全面总结；Jouse(1963)，关于西北太平洋不同水团下地区深海岩心硅藻地层的讨论；Jouse (1969, 1971a)，关于在北太平洋40°N以北的一些岩心（包括V20-119长岩心）中观察到的硅藻数量、生态和系统发育三种类型的变化；Muchina(1969, 1971)，研究了许多深海岩心中的硅藻地层，其中包括太平洋赤道部分穿透上新世沉积物的两个岩心。Kanaya（1961）和Kanaya and Koizumi（1966）也对北太平洋现代深海沉积物中硅藻的地理分布进行了研究。Kanaya和Koizumi（1966）在北太平洋V20-130长岩心中定义了一个统计值Td（硅藻温度）值，并讨论了硅藻组合结构在岩心中由上部到下部的变化。小泉（1970a, b）报道了日本海大和盆地和菲律宾海四国盆地晚第四纪地表水温度的波动，这是由几个深海岩心中的硅藻所显示的。Donahue（1970）以古地磁地层学为时间尺度定义了上新世-更新世晚期硅藻生物地层带，并利用北太平洋北部深海岩心的Td值讨论了气候变化。Burckle（1972）参考赤道太平洋的硅藻地层学，将选定的上新世-更新世硅藻的产状与古地磁和其他微化石地层学（Hays et al., 1969）进行了比较，后来定义了赤道东太平洋沉积物中新世晚期至新近的硅藻带。Kanaya（1971）研究了副热带太平洋实验莫霍层序的硅藻组合，并将该层序与瑞典深海芯76进行了对比。
A large area of the sea floor of the North Pacific is occupied by siliceous sediments containing microfossils such as diatoms, silicoflagellata, and Radiolaria (Lisitsyn 1971). These siliceous sediments mainly consist of diatom valves, amorphous biogenous silica, except in the zone of radiolarian ooze north of the equator, around 10°N latitude (Riedel, 1959). The quantitative distribution of diatom valves in a unit weight of surface sediment layer of the Pacific Ocean was summarized by Jouse et al. (1969,1971). The micropaleontological studies on the cores from the North Pacific, owing to the lack of good carbonate components have been carried out in the field of siliceous microfossils, especially of diatoms. The first report on diatom stratigraphy in deep-sea cores from the North Pacific was done by Kolbe (1954). He showed that Tertiary species were restricted to the lower levels of core 76, taken by the Swedish Deep-Sea Expedition from the equatorial part of the Pacific, and that there is a distinct difference between the lower and upper parts of the core. Since Kolbe, a number of workers from the Soviet Union have been very active in the study of the diatoms in the deep-sea cores from the North Pacific and its neighboring seas; namely the Bering Sea, the Sea of Okhotsk, and the Sea of Japan. Through their systematic researches, the Russian workers have become convinced (e.g. Jouse, 196Id, 1962) that (a) the diatom thanatocoenoses in the uppermost layer of the bottom sediments depend to a large extent on the biocoenoses in the water masses above, (b) the species composition reflects the Oceanographic conditions in the overlying water masses, (c) the geographical zonality of diatom assemblages in bottom sediments is well expressed in their present distribution in the Pacific Ocean, (d) climatic variations during the Quaternary caused the displacement of biogeographical zones in the ocean, synchronous with displacements of the upper water masses, and therefore (e) one may judge the thermal conditions at the time during the accumulation of sediments from the changes in the composition of diatom species (Jouse 196Id). Reports on the diatom stratigraphy of deep-sea cores are as follows: Seczkina (1959), on the diatoms in a long core from the Sea of Japan; Jousé (1961a, b), on the correlation of horizons marked by diatoms in long cores from the northwestern part of the Pacific; Jouse (1962), a thorough summary of diatom studies carried out by Russian workers in the Soviet Far East seas (Bering Sea, the Sea of Okhotsk, the Sea of Japan, and the northwestern part of the North Pacific); Jouse (1963), on the discussion of diatom stratigraphy of the deep-sea cores from the areas under different water masses in the northwestern Pacific; Jouse (1969, 1971a), on the three types of diatom variation — quantitative, ecological, and Phylogenetic — observed in some cores, including a long core, V20-119, from north of 40°N in the North Pacific; Muchina (1969, 1971), on the diatom stratigraphy in many deep-sea cores, including two cores from the equatorial parts of the Pacific which penetrated Pliocene sediments. The geographical distribution of diatoms in modern deep-sea sediments of the North Pacific was also studied by Kanaya (1961) and Kanaya and Koizumi (1966). Kanaya and Koizumi (1966) defined a statistic, Td (diatom temperature) values, in the long core V20-130 from the North Pacific and discussed the fact that the structures of the diatom assemblages change from the upper part to the lowermost part in the core. Koizumi (1970a, b) reported the fluctuations of surface water temperatures during the late Quaternary in the Yamato Basin of the Sea of Japan and the Shikoku Basin of the Philippine Sea, as shown by diatoms in several deep-sea cores. Donahue (1970) defined diatom biostratigraphic zones in the late PliocenePleistocene by using paleomagnetic stratigraphy as a time scale and discussed climatic changes by the use of the Td values in deep-sea cores from the northern North Pacific. With reference to the diatom stratigraphy in the equatorial Pacific, Burckle (1972) compared the occurrence of selected Plio-Pleistocene diatoms with the paleomagnetic and other microfossil stratigraphy (Hays et al., 1969) and later defined a late Miocene to Recent diatom zonation for eastern equatorial Pacific sediments. Kanaya (1971) studied the diatom assemblages of the experimental Mohole sequence from the subtropical Pacific and correlated the sequence with the Swedish deep-sea core 76.