印尼外海沉积序列及相关的沉积事件
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摘要
印尼位于板块缝合带,地质构造复杂,是地球上最为活跃的构造带之一,成为地震、海啸和火山爆发等灾变事件的多发区。这些事件所形成的事件沉积广泛保存于印尼陆上及其周边海域海底的沉积物中,使得该区成为沉积事件研究的热点区域。深海环境的沉积以远洋或半远洋沉积为主,沉积速率较低,沉积相对稳定和纯粹,是长尺度古沉积事件研究的理想场所。本文以印尼周边海域深海沉积岩心(IR-GC1)为研究对象,在原有研究基础上,开展沉积学、地层学、古海洋学相关研究,揭示该海区古沉积事件,建立可靠的年龄框架,并探讨这些事件的形成机制及其对深海沉积物特征的影响。通过综合分析,获得了以下结论和认识：
研究区沉积物组分以粉砂为主,沉积物类型主要为粘土质粉砂以及含粘土粉砂砂质泥。沉积物岩心的岩性特征、粒度特征及元素地球化学分布在垂向上变化显著,反映了沉积环境曾经发生过突变。
利用氧同位素地层法,外加新仙女木变冷事件层和粉红色红拟抱球虫的末现面作为年代控制点,获得沉积物岩心底部年龄约为136ka,为晚更新世以来的沉积,平均沉积速率为1.23cm/ka,表现为低沉积速率半远洋沉积的特点。通过垂向比较识别出4期相对快速堆积事件,分别发生在90.1-82.0ka,75.0-70.9ka,54.8-50.4ka和20.0-11.6ka期间。并且识别出1期沉积间断事件,发生在距今118-109ka,它与浊流事件的冲刷有关。
以沉积物粒度特征突变为主要指标,通过粒度参数的垂向变化、粒度频率曲线和概率累积曲线特征,识别出7个深海浊积层,分别对应7个浊流沉积事件,发生年代分别为：130-128ka,107-105ka,100-98ka,87-86ka,53-50ka,41-37ka,29-20ka。整个IR-GC1岩心中,深海浊流出现的频率可达54次/Ma,浊流层的总厚度达28cm,约占岩心沉积总量的16.7%。因此,该区的深海浊流事件异常发育,对正常深海沉积影响显著。
深海浊流沉积具有粒径粗、分选差、峰态宽、频率曲线呈双峰态、沉积突变明显等特征。另外,粒度分级也是深海浊流沉积的重要特征,可作为识别浊积层的一个重要标志。
在IR-GC1岩心中识别出3个火山灰层,它们富含火山玻璃和长石、云母及角闪石等矿物颗粒。综合火山玻璃的形貌、化学成分及其年代,认为层A来源于末次Toba火山喷发。层B成分上与层A几乎一致,认为其可能代表层A的底部,与海底滑塌、海洋底流或生物扰动对沉积物的改造有关。而层C与层A,B成分上有差异,表明它们岩浆来源不同,其具体的来源还无法确定。另外,研究发现SiO2/Al2O3和K2O/A12O3比值可以作为沉积物中酸性火山灰沉降事件的指标。
印尼外海13.6万年以来沉积事件异常发育,其触发机制包括海啸、地震和火山爆发事件以及与冰川作用有关的海平面变化。其中,发生在130-128ka期间的深海浊流沉积事件归因于海平面的快速上升；发生在107-86ka期间的3次深海浊流沉积事件由海啸、地震等突发事件触发；而发生在53-20ka期间的3次深海浊流沉积事件则受低海平面所控制,该时期海平面下降,河口深入陆架,其搬运的陆源物质向陆架深部甚至陆坡倾泻,使得陆架边缘碎屑堆积物的稳定性极易遭受破坏,从而发生坍塌引发大规模的浊流。另外,发生在80-76ka和134ka附近的火山降落沉积事件则与巽他岛弧重大的火山喷发事件有关。
The plate tectonic setting of Indonesia is complex, and catastrophic geologic events have likely been plentiful. Event deposits induced by those catastrophic events have been widely preserved in sediments of the land and seabed. The deep-sea basin in this region is mainly documented by pelagic and himipelagic sedimentation. So the sedimentation rate of the deep-sea basin is relatively low. Thus, it can be served as an ideal situation to the long-term research on sedimentary events.
Based on existing research, this paper is done to systematically analyze the sedimentary sequences of the core IR-GC1from abyssal sediments off Indonesia, recognize the sedimentary events recorded in the sediments, and discuss their trigger mechanism.
Through comprehensive analysis, results obtained as follow:
The sediment is mainly composed of clayey silt and clay-silt-containing sandy mud. The lithology, grain size and element geochemistry in the vertical direction changes significantly, suggesting that the sedimentary environment have occurred mutation.
The age model for core IR-GC1was established mainly by oxygen isotope stratigraphy. Additional age markers, such as the last appearance datum (LAD) of pink-pigmented Globigerinoides ruber (127ka BP) and the occurrence of Younger Dryas cooling event (12.68-11.59ka BP), were also used for age control. Hence, the base of core IR-GC1was determined to ca.136ka. The average sedimentation rate was1.23cm/ka. Four period of relatively rapid deposition, respectively, occurred in90.1-82.Oka,75.0-70.9ka,54.8-50.4ka, and20.0-11.6ka. A sedimentary hiatus occurred in118-109ka, which is related to the erosion by turbidity current.
Using the mutation of particle size characteristics as the main indicator, seven deep-sea turbidite layers can be clearly identified, corresponding to seven deposition events occurred in130-128ka,107-105ka,100-98ka,87-86ka,53-50ka,41-37ka, and 29-20ka respectively. The total thickness of the turbidite layers up to28cm, which is about30%of the core length. Deep-sea turbidite deposition is characterized by coarse grain size, poor sorting, wide kurtosis, bimodal frequency curve, and deposition mutation. In addition, particle size classification is also an important feature of deep-sea turbidite deposition, which can be used as an indicator to identify the turbidite layer.
Three volcanic ash layers were identified from core IR-GC1. They were dominated by glass shards with minor mineral crystals, such as plagioclase, biotite, and hornblende. According to the morphology and major element compositions of the representative glass shards, we suggest that ash layer A is correlated to the youngest Toba Tuff (YTT,80-76ka). Layer B is thought to be a basal part of layer A and could be the result of reworking of the sediments by slumping, bottom currents, or bioturbation. Ash layer C bear different geochemistry characteristics of layers A and B suggesting it was not originated from Toba but recorded another eruption event of high-silica rhyolite in the region. In addition, SiO2/A12O3and K2O/A12O3ratio can be used as a marker for acid volcanic ash deposition events.
Over the past136ka, turbidite deposition events occurred frequently in deep-sea off Indonesia. The possible trigger mechanism including tsunamis, earthquakes, volcanic eruptions and sea-level change.
研究区沉积物组分以粉砂为主,沉积物类型主要为粘土质粉砂以及含粘土粉砂砂质泥。沉积物岩心的岩性特征、粒度特征及元素地球化学分布在垂向上变化显著,反映了沉积环境曾经发生过突变。
利用氧同位素地层法,外加新仙女木变冷事件层和粉红色红拟抱球虫的末现面作为年代控制点,获得沉积物岩心底部年龄约为136ka,为晚更新世以来的沉积,平均沉积速率为1.23cm/ka,表现为低沉积速率半远洋沉积的特点。通过垂向比较识别出4期相对快速堆积事件,分别发生在90.1-82.0ka,75.0-70.9ka,54.8-50.4ka和20.0-11.6ka期间。并且识别出1期沉积间断事件,发生在距今118-109ka,它与浊流事件的冲刷有关。
以沉积物粒度特征突变为主要指标,通过粒度参数的垂向变化、粒度频率曲线和概率累积曲线特征,识别出7个深海浊积层,分别对应7个浊流沉积事件,发生年代分别为：130-128ka,107-105ka,100-98ka,87-86ka,53-50ka,41-37ka,29-20ka。整个IR-GC1岩心中,深海浊流出现的频率可达54次/Ma,浊流层的总厚度达28cm,约占岩心沉积总量的16.7%。因此,该区的深海浊流事件异常发育,对正常深海沉积影响显著。
深海浊流沉积具有粒径粗、分选差、峰态宽、频率曲线呈双峰态、沉积突变明显等特征。另外,粒度分级也是深海浊流沉积的重要特征,可作为识别浊积层的一个重要标志。
在IR-GC1岩心中识别出3个火山灰层,它们富含火山玻璃和长石、云母及角闪石等矿物颗粒。综合火山玻璃的形貌、化学成分及其年代,认为层A来源于末次Toba火山喷发。层B成分上与层A几乎一致,认为其可能代表层A的底部,与海底滑塌、海洋底流或生物扰动对沉积物的改造有关。而层C与层A,B成分上有差异,表明它们岩浆来源不同,其具体的来源还无法确定。另外,研究发现SiO2/Al2O3和K2O/A12O3比值可以作为沉积物中酸性火山灰沉降事件的指标。
印尼外海13.6万年以来沉积事件异常发育,其触发机制包括海啸、地震和火山爆发事件以及与冰川作用有关的海平面变化。其中,发生在130-128ka期间的深海浊流沉积事件归因于海平面的快速上升；发生在107-86ka期间的3次深海浊流沉积事件由海啸、地震等突发事件触发；而发生在53-20ka期间的3次深海浊流沉积事件则受低海平面所控制,该时期海平面下降,河口深入陆架,其搬运的陆源物质向陆架深部甚至陆坡倾泻,使得陆架边缘碎屑堆积物的稳定性极易遭受破坏,从而发生坍塌引发大规模的浊流。另外,发生在80-76ka和134ka附近的火山降落沉积事件则与巽他岛弧重大的火山喷发事件有关。
The plate tectonic setting of Indonesia is complex, and catastrophic geologic events have likely been plentiful. Event deposits induced by those catastrophic events have been widely preserved in sediments of the land and seabed. The deep-sea basin in this region is mainly documented by pelagic and himipelagic sedimentation. So the sedimentation rate of the deep-sea basin is relatively low. Thus, it can be served as an ideal situation to the long-term research on sedimentary events.
Based on existing research, this paper is done to systematically analyze the sedimentary sequences of the core IR-GC1from abyssal sediments off Indonesia, recognize the sedimentary events recorded in the sediments, and discuss their trigger mechanism.
Through comprehensive analysis, results obtained as follow:
The sediment is mainly composed of clayey silt and clay-silt-containing sandy mud. The lithology, grain size and element geochemistry in the vertical direction changes significantly, suggesting that the sedimentary environment have occurred mutation.
The age model for core IR-GC1was established mainly by oxygen isotope stratigraphy. Additional age markers, such as the last appearance datum (LAD) of pink-pigmented Globigerinoides ruber (127ka BP) and the occurrence of Younger Dryas cooling event (12.68-11.59ka BP), were also used for age control. Hence, the base of core IR-GC1was determined to ca.136ka. The average sedimentation rate was1.23cm/ka. Four period of relatively rapid deposition, respectively, occurred in90.1-82.Oka,75.0-70.9ka,54.8-50.4ka, and20.0-11.6ka. A sedimentary hiatus occurred in118-109ka, which is related to the erosion by turbidity current.
Using the mutation of particle size characteristics as the main indicator, seven deep-sea turbidite layers can be clearly identified, corresponding to seven deposition events occurred in130-128ka,107-105ka,100-98ka,87-86ka,53-50ka,41-37ka, and 29-20ka respectively. The total thickness of the turbidite layers up to28cm, which is about30%of the core length. Deep-sea turbidite deposition is characterized by coarse grain size, poor sorting, wide kurtosis, bimodal frequency curve, and deposition mutation. In addition, particle size classification is also an important feature of deep-sea turbidite deposition, which can be used as an indicator to identify the turbidite layer.
Three volcanic ash layers were identified from core IR-GC1. They were dominated by glass shards with minor mineral crystals, such as plagioclase, biotite, and hornblende. According to the morphology and major element compositions of the representative glass shards, we suggest that ash layer A is correlated to the youngest Toba Tuff (YTT,80-76ka). Layer B is thought to be a basal part of layer A and could be the result of reworking of the sediments by slumping, bottom currents, or bioturbation. Ash layer C bear different geochemistry characteristics of layers A and B suggesting it was not originated from Toba but recorded another eruption event of high-silica rhyolite in the region. In addition, SiO2/A12O3and K2O/A12O3ratio can be used as a marker for acid volcanic ash deposition events.
Over the past136ka, turbidite deposition events occurred frequently in deep-sea off Indonesia. The possible trigger mechanism including tsunamis, earthquakes, volcanic eruptions and sea-level change.
引文
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