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Paleoenvironmental implications of the calcium isotope characteristics in the MD81349 from the Nintyeast Ridge in the Indian Ocean
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Feng WANG1, Nianqiao FANG2, *, Chaoyong HU3, Sarah GOLDSMITH4, Yonghang XU1, Xuan DING2, Aijun WANG1, Ping CHEN5, Rui BAO6
Acta Oceanologica Sinica | 2018, 37(9) : 59 - 66
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Acta Oceanologica Sinica | 2018, 37(9): 59-66
• Marine Geology •
Paleoenvironmental implications of the calcium isotope characteristics in the MD81349 from the Nintyeast Ridge in the Indian Ocean
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Feng WANG1, Nianqiao FANG2, *, Chaoyong HU3, Sarah GOLDSMITH4, Yonghang XU1, Xuan DING2, Aijun WANG1, Ping CHEN5, Rui BAO6
Affiliations
  • 1 Third Institute of Oceanography, State Oceanic Administration, Xiamen 361005, China
  • 2 Institute of Marine Geology and Geophysics, China University of Geosciences (Beijing), Beijing 100083, China
  • 3 School of Earth Sciences, China University of Geosciences, Wuhan 430074, China
  • 4 Demo Laboratory, Ctd. MicroMass, Mantchestt M139PL, United Kingdom
  • 5 School of Earth Science Environmental Engineering, Anhui University of Science and Technology, Huainan 232001, China
  • 6 Climate and Environment Sciences Laboratory of the institute Pierre Simon Laplace (LSCE), Gif sur Yvette 75000, France
Published: 2018-09-25 doi: 10.1007/s13131-018-1264-7
Outline
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A δ44Ca curve from shells of the planktonic foraminifera Globigerinoides sacculifer in calcareous biogenic oozes has been extracted from the Nintyeast Ridge in the Indian Ocean since 300 ka. By combining terrigenous inputs (e.g., grain size, magnetic susceptibility, and turbidite frequency) with the oceanic productivity (e.g., biogenic content and Neogloboquadrina dutertrei content), it is found that the curve’s variations are closely related to the historical evolution of the oceanic calcium cycle. The δ44Ca value is in lower tendency and has small oscillation during Marine Isotope Stage (MIS) 6, when the supply of terrigenous detrital is highest. In contrast, during MIS 3, 5 and 7, the δ44Ca values are in higher tendency, and their fluctuations are consistent with the variations of the productivity proxies. These results suggest that the calcium isotopes are mainly influenced by the input of the Himalayan erosion products to the northern Indian Ocean. In addition, the developmental stages of calcareous planktons may have a secondary impact on the fluctuations of the calcium isotope ratio of sea water.

Nintyeast Ridge  /  calcium isotope  /  paleoceanography  /  Indian Ocean
Feng WANG, Nianqiao FANG, Chaoyong HU, Sarah GOLDSMITH, Yonghang XU, Xuan DING, Aijun WANG, Ping CHEN, Rui BAO. Paleoenvironmental implications of the calcium isotope characteristics in the MD81349 from the Nintyeast Ridge in the Indian Ocean[J]. Acta Oceanologica Sinica, 2018 , 37 (9) : 59 -66 . DOI: 10.1007/s13131-018-1264-7
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1 Introduction
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The variations of light isotope ratios, such as those of oxygen and carbon, have positive correlations with paleoceanographic conditions. In contrast, calcium isotopes of the paleoenvironmental implications are not well constrained (e.g., Russell et al., 1978; Skulan et al., 1997; De La Christina and DePaolo, 2000; Farkaš et al., 2007; Griffith et al., 2008a). Calcium is an important component of the pelagic plankton shells that participate in the cycles of a lithosphere, a hydrosphere and a biosphere, however, the calcium isotopic fractionation characteristics during sedimentation are still limited (Farkaš et al., 2007; Griffith et al., 2008a; Fantle, 2015). The 44Ca to 40Ca fractionation effect due to biological activity and variations in the water temperature during carbonate precipitation has drawn significant attention over the past decade (e.g., Skulan et al., 1997; Zhu and Macdougall, 1998; Nägler et al., 2000; Gussone et al., 2004, 2009; Hippler et al., 2006; Griffith et al., 2008a, b; Kısakürek et al., 2011).
There are six stable isotopes of calcium in nature, 40Ca (96.941%), 42Ca (0.647%), 43Ca (0.135%), 44Ca (2.086%), 46Ca (0.004%) and 48Ca (0.187%). On the basis of the abundances, fractionation characteristics and detection precision of each isotope, the ratio of 44Ca abundance to 40Ca is a widely used proxy for a paleoenvironmental analysis (Heuser et al., 2002; Gussone et al., 2005; Schiller et al., 2012).
Ca2+ in the ocean mainly originates from the terrigenous input, the eruption of suboceanic basaltic lava, and hydrothermal activity. Ca2+ precipitates from sea water mainly through biological activity and forms calcium carbonate. Imbalances between the input and output of calcium causes variations of the Ca2+ concentration in sea water and may also lead to the fluctuations of the 44Ca/40Ca ratio (De La Christina and DePaolo, 2000). Skulan et al. (1997) suggested that the δ44Ca value of basaltic rocks was approximately 0, the δ44Ca value of sea water was approximately 0.90×10–3, and the δ44Ca value of biological calcareous shells was approximately 1.00×10–3 lower than that of the surrounding sea water. De La Christina and DePaolo (2000) showed that the δ44Ca values of modern seawater fluctuate between 0.80×10–3 and 0.92×10–3. The average δ44Ca value of the hydrothermal fluids that are associated with mid-ocean ridge basalt (MORB) is –0.61×10–3. Differences in the petrological characteristics and degree of weathering of terrigenous matters lead to large differences in the δ44Ca values in different river basins. For example, the δ44Ca values vary from –0.63×10–3 in the Changjiang (Yangtze) River to –1.68×10–3 in the Ganges. The δ44Ca values of the calcareous shells of foraminifera and coccolithophores correlate well with that of the surrounding seawater but are generally 1.20×10–3–1.30×10–3 lower; the δ44Ca values of corals and Holocene carbonate oozes are even lower, with an average of –2.15×10–3. The δ44Ca values of organic bodies show that the lighter Ca2+ are preferentially taken up and fixed in shells, which causes a positive shift of the residual δ44Ca value in the surrounding sea water compared with the initial value. These characteristics can be used to develop a general model of the oceanic calcium cycle and calcium isotope fractionation (Fig. 1).
When carbonate matter precipitates from sea water, the effect of the water temperature has attracted much attention. Skulan et al. (1997) proposed that the δ44Ca values of the foraminifera shells were related to the temperature, but the relationship was very weak. In contrast, De La Christina and DePaolo (2000) proposed that the δ44Ca features of foraminifera shells were not related to the seawater temperature. Zhu and Macdougall (1998) noted that the 44Ca/40Ca values in the shells of shallow-water planktonic foraminifera such as Globigerinoides sacculifer and Neogloboquadrina pachyderma tended to be heavier during the warm period (Holocene) than during colder periods and in deep water. On the basis of an analysis of the calcium isotopes of cultured living foraminifera and ancient foraminifera shells, Nägler et al. (2000), Sime et al. (2005) and Gussone et al. (2003, 2004) concluded that the δ44Ca values of the calcareous of foraminifera were related to the temperature of the sea water in which they grew due to fractionation. Thus, the temperature effect on the calcium isotopic fractionation that is observed in laboratories cannot be ignored. However, calcium isotopes curve obtained in core is affected by kinds of interferences and bondages, including a variety of factors composite. To make clear which factors dominant the calcium isotopes curve significantly, we need to conduct detailed analyses based on the actual conditions. We selected a single species of foraminifera (G. sacculifer) from the northern Indian Ocean and measured its 44Ca/40Ca ratios with a multiple-collector inductively coupled plasma mass spectrometer (MC-ICP-MS). Then we got a δ44Ca curve that spans 300 ka and discussed the characteristics of the calcium isotope variations of the foraminifera shells and their geological implications in paleoenvironment.
2 Materials and methods
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The foraminifera shells were collected from a 4.3 m core (MD81349) in the Nintyeast Ridge (01°01′S, 89°22′E, water depth of 2 505 m) (Fig. 2). The foraminifera content in the MD81349 core was significantly higher than that of cores from the nearby ODP758, DSDP216 and DSDP217 stations. The information of sites involved in this study is in Table 1. The oxygen and carbon isotope from the shells of G. ruber have been tested at the Climate and Environment Sciences Laboratory of the Institute Pierre Simon Laplace (LSCE) and the National Centre of Scientific Research (CNRS) in France. Biological particles and N. dutertrei content data have been finished at the Institute of Marine Geology and Geophysics, China University of Geosciences (Beijing).
In this study, we collected samples from the MD81349 core every 5 cm in the same layers with the oxygen and carbon isotope analysis. A total of 92 samples were collected from the core. Each sample was carefully rinsed and ten G. sacculifer individuals with sizes of 315–425 μm were selected, rinsed with deionized water three times, and subjected to ultrasonication for 3 min. We then dissolved them in 8 mL of 5% HNO3 solution in a teflon bottle and put the solution in the MC-ICP-MS to measure the calcium isotope ratios. The sample analysis was conducted at the Demonstration Laboratory of the MicroMass Company in Manchester, UK. We put 3 mL of the fully dissolved solution in the special sample chamber of the instrument and set up the measurement parameters to count the number of atoms with mass numbers of 39.0, 40.0, 42.0, 43.0, 43.5 and 44.0. The analysis procedure followed the repeating sequence of standard-sample-standard-sample. The raw data were first corrected for potassium interference to determine the concentration of 40Ca in the solution. The data were then corrected for strontium (Sr2+) Sr2+ inferences on the Ca isotopes using the 43.5 signal (corresponding to Sr2+) to determine the concentrations of 44Ca, 43Ca and 42Ca in the same solution. Finally, the data were calibrated using NIST SRM915 a (Standard Reference Materials 915 a, National Institute of Standards and Technology, US Department of Commerce) as the standard reference to obtain the 44Ca and 40Ca data and to yield the curve that represents the variation in δ44Ca since 275 ka. The resolution of δ44Ca measurement is lesser than 0.01%。
3 Results
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The ridge sediment was mainly composed of marine biogenic matter. In the past 250 ka, a deposition rate was generally 1.0–2.0 cm/ka (Fang, 1987). On the basis of previous studies (Foucault and Fang, 1987; Ding et al., 1999, 2000, 2003; Fang et al., 2001a, 2002, 2004, 2009), the ridge sediment sequence that is contained in the MD81349 core was continuous and contains many environmental signals that can be used for global comparisons or that reflect significant regional events.
The δ18O curve, which can be used to distinguish eight oxygen isotope stages (Fig. 3), corresponded well to that of the LR04 stack (Lisiecki and Raymo, 2005) . Our δ18O curve was also supported by chronological evidence from the Toba ash layer (75 ka) at a depth of 121–126 cm and the last-appearance datum of pink G. ruber (128 ka) in the study area (Ninkovich et al., 1978; Fang, 1990; Paillard et al., 1996).
The main δ44Ca values range from –0.29×10–3 to 1.02×10–3. The maximum value of the δ44Ca curve for the G. sacculifer shells in the Core MD81394 is 1.52×10–3 (in MIS 5.5), and the minimum is –0.99×10–3 (in MIS 6.2) (Table 2). The variation curve which takes on low tendency in the glacial periods but high tendency in the interglacial periods does not show fully corresponding to the glacial-interglacial cycles (Fig. 4). In addition, the δ13C curve of the foraminifera shells do not entirely correspond to the glacial/inter-glacial alternations. This phenomenon is due to the oceanic productivity. The values of biological content range from 1 200 to 15 000 g–1. The high value is in the interglacial periods, while the low value in the glacial periods. There is a biological event in 160 ka when the biological particles content value is the lowest. N. dutertrei content, as one of the effective productivity proxies, changed mainly same with biological content (Fig. 4).
4 Discussion
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In the research of the northern Indian Ocean sedimentary records since 300 ka, the predecessors (Fang et al., 2004, 2009) have pointed out that the MIS 6 is the most significant period which is characterized by the strongest terrigenous input and the remarkable ecological events. In our study, the characteristic of δ44Ca also can be interpreted to the latest evidence for this view.
Generally, the basic characteristics of the δ44Ca curve take on the low tendency in the glacial periods, the high tendency in the interglacial periods, but peak value is not consistent with an oxygen isotope change curve, which is focused on discussing in our study (Fig. 4).
There are two different kinds of sedimentary types in the northern Indian Ocean: Bengal Fan sedimentary type and Nintyeast Ridge sedimentary type. The former is mainly Himalayan erosion which carried by turbidity; the latter is pelagic sediments which is the calcareous ooze. Although their compositions and sedimentary types are great difference, their sedimentary processes are influenced all together by the regional tectonic uplift, the sea level change and chemical properties of sea (Fang et al., 2009). Thus, the sedimentary processes can refer to each other. In our study, the core we research is from the Nintyeast Ridge, which does not suffer the turbidity activity directly. In order to explore the control factors of δ44Ca, we widely cited the predecessors’ results in the Bengal fan as a reference, such as magnetic susceptibility, grain size, turbidite layers (proxy), which can reflect terrigenous input change.
Although the overall pattern of low values in the glacial periods and high values in the interglacial periods prior to MIS 4.0 is similar to the oscillation of the δ18O curve and represents climatic cycles. What interests us is that, the peak positions of the two curves differ greatly. It indicates that the δ44Ca values in the foraminifera shells are not closely related to cold and warm conditions during MIS 5.5, which is characterized as a typical warm climate in the δ18O curve. For example, the relationship between the δ44Ca curve and the glacial/interglacial alternations since MIS 4.0 is unclear. MIS 5.5 generally follows the low-value characteristics of MIS 6.0, and MIS 5.4 and 5.3 contain the maximum peak value of the entire record. From MIS 5.3 to the early part of MIS 3.0, the curve is relatively flat but has some rhythmic characteristics. During MIS 3.0 and 2.0, the trend of the δ44Ca curve is generally opposite to that of the δ18O curve; however, during the Holocene, the δ18O curve contains a negative peak value because of the global glacial retreat, but the δ44Ca curve remains at intermediate levels. It is well known that the δ18O curve is a signal corresponding to the variations of SST and global ice sheet, characterized by oscillating between the glacial periods and the interglacial periods. With reference to Fig. 4, we can see that the oscillation characteristic of our δ44Ca curve can vary with the δ18O one neither on the whole nor in detail. As a result, we argue that the SST may bring little influence to the pattern of δ44Ca curve.
There are several explanations for this observation. (1) Although the experimental results of Nägler et al. (2000) indicate that δ44Ca varies due to the water temperature, their study only shows reactions under simple laboratory conditions that are not representative of the synergistic environmental effects under complex natural conditions. If their conclusion that every 1°C change in temperature is equivalent to a variation of (0.24±0.02) δc(44Ca) is directly applied to estimating the surface sea temperature of the Indian Ocean over the past 200 ka, the maximum temperature difference could be 6.0–11.0°C, which is not realistic and thus is hard to accept. (2) The δ44Ca curve does not display any significant peaks during warm periods such as the Holocene and MIS 5.5. In contrast, the δ44Ca curve contains an interval with prominent high values around the last glacial maximum. (3) During several transition zones of the glacial/interglacial periods, such as the MIS 8.0, 7.0 and 4.0 transitions, the peak δ44Ca values cannot be explained by increasing the surface sea temperature.
As is showed by the overall fluctuations of the δ44Ca curve in the MD81349 core, the primary controlling factor should be related to the operation of the oceanic calcium cycle system. Skulan et al. (1997) and Zhu and Macdougall (1998) specifically addressed the issue of the calcium cycle. Owing to the different standards that they used, they obtained different δ44Ca values for the background sea water, ocean ridge basalt, hydrothermal fluids, ancient carbonate rocks, aluminosilicate minerals, river discharges and modern organism skeletons (shells) (Fig. 1). However, they shared several common characteristics. The δ44Ca values were highest in the sea water, and the δ44Ca values of the ocean-floor volcanic eruption products were lower than that of sea water but higher than those of other calcium-rich materials. In addition, the δ44Ca values were lowest in carbonate rocks (sediment), which were mainly controlled by biological sedimentation. In addition, the data of Skulan et al. (1997) show that the input of terrigenous erosion products from river systems to the ocean can generate very low δ44Ca values. De La Christina and DePaolo (2000) showed that the disequilibrium between terrigenous erosion products and biogenic sedimentation could cause a significant drift in the Ca2+ isotope composition of sea water. The variations in the ratio between the terrigenous Ca input flux due to weathering and the Ca output flux of biogenic sedimentation in the ocean over the past 80 Ma that they obtained showed a significant reverse evolutionary relationship to the marine carbonate δ44Ca record(De La Christina and DePaolo, 2000). The δ44Ca values in rocks were approximately –0.44×10–3 and reached 0 during the late Eocene (ca. 40 Ma). However, from the Oligocene to the mid-Miocene (ca. 34–15 Ma), the input of light calcium components far exceeded the precipitation of light calcium components by the skeletons and shells of calcareous marine organisms due to the significant increase in the weathering and denudation of terrigenous carbonate rocks and the enhanced input of calcium-bearing erosion products to the oceans. Therefore, the δ44Ca record contains a low-value interval that lasts for nearly 20 Ma. Hodell and Woodruff (1994) note that the 87Sr/86Sr ratio in the sea water contain a period of rapid increases between 20 and 16 Ma, which indicate that terrigenous erosion and discharge from the Himalaya and the Tibetan Plateau significantly impact the oceanic chemical components.
The 44Ca curve characteristics of high values in the (sub-) interglacial periods and low values in the (sub-) glacial periods during MIS 5.0–8.0 (Fig. 4) may also be related to the variations in the terrigenous input flux to the northern Indian Ocean. The 44Ca value in carbonate materials are lower than that provided by silicates. Himalayan erosion products is carried to the whole Ganges delta(Fang, 1990, 2001a). Owing to the uplift of the Tibetan Plateau and the large exposure of carbonate rocks in the Greater Himalaya, the terrigenous input of the Ganges was characterized by extremely low 44Ca values. The sedimentary record of the Bengal deep-sea fan shows that the amount of terrigenous input is controlled by glacial sea-level variations (Foucault and Fang, 1987; Fang, 1990). This suggests that enhanced rock weathering during (sub-) glacial periods, especially the large amounts of erosion products that are carried across the continental shelf to pelagic regions, would inevitably decrease the δ44Ca value of the sea water. In contrast, as the sea level rises during (sub-) interglacial periods, the terrigenous input fluxes to the oceans decrease, and thus, the 44Ca in the seawater is likely to remain high. Note that all of the sedimentary records in the northern Indian Ocean show that the intensity of the terrigenous input during MIS 6.0 was the highest of the past 300 ka (Fig. 5). Fang et al. (2001a) pointed out that the terrigenous input is carried by the turbidity current to the south of 10°S in the Indian Ocean Basin, which reflects the turbidite activity influences widely in our study area. Turbidite activity is dominated by terrigenous input activities. When the turbidite layers appear, it means the terrigenous input to the ocean. Although the turbidite layer does not appear in the Core MD81349 directly, the sedimentary process of Core MD81349 is also affected by the terrigenous input. Through the turbidite layer records in the other cores of the Bengal Fan which can illustrate the terrigenous input to the Bengal Fan (Fig. 5), we can see that the Cores MD77181, MD77190 and MD81345 have the turbidite layers in MIS6.0. The grain size and the calcium carbonate content show that the terrigenous input has a strong influence on our study area in MIS 6.0 and a biological event happened in 160 ka (Fang et al., 2001a; Zhang, 2002). The significant ecological events between 169 and 160 ka led to a severe oceanic productivity crisis in the study area (Fang et al., 2001b, 2004). The anomalously high input and low output of Ca led to an interval of low δ44Ca values during MIS 6.0 (Figs 4 and 5). As we know, the terrigenous input means a plenty of compound of iron, such as magnetite are carried into the sediment, magnetic susceptibility corresponding appears high value. Figure 5 shows that when the magnetic susceptibility of MD77181, MD77180 and MD77169 is high value in MIS 6.0, the δ44Ca takes on the low tendency, which demonstrates the terrigenous input makes the δ44Ca value low. Meanwhile, the turbidite activity of the MD77181, MD77190 and MD81345 intensively in MIS 6.0 which are dominated by the terrigenous transport activities also prove that the amount of the terrigenous input in MIS 6.0 lead to the low δ44Ca in our study area. The transport of terrigenous carbonate weathering products to the ocean mainly occurs through real ionic solutions and rarely leaves a visible sedimentary record in the oceans as silicate; therefore, the 44Ca/40Ca ratio in calcareous shells could be an effective monitoring proxy for the terrigenous carbonate input.
The factors that affect the δ44Ca curve after MIS 5.0 are more complicated. The glacial sea-level cycles continue to affect the terrigenous input and ultimately control the δ44Ca variations in the foraminifera shells. However, the developmental stages of biogenic sediments affected the final results (i.e., the feedback of the new distribution of δ44Ca in the sea water to the shell record). In fact, during MIS 6.0 and 7.0, the productivity underwent significant fluctuations (Fang et al., 2004). However, due to the large differences in the terrigenous input fluxes, the δ44Ca characteristics of the foraminifera shells are not consistent. For example, during MIS 7.1 (ca. 200 ka), the sedimentary records in the northern Indian Ocean generally show increasing trends of oceanic productivity, of which the main characteristics include more abundant planktonic foraminifera and radiolarians, higher N. dutertrei contents in the plankton foraminifera, and increased Gd/Ca ratios in the calcareous shells. During this period, because of the low terrigenous input, the effect of the high productivity produced peak zones in the δ44Ca that were recorded by organism shells. Nonetheless, due to the increase in the terrigenous input during MIS 6.0 and despite the significantly higher productivity than in MIS 7.0 during certain periods, the discharge of 40Ca-rich continental erosion products in the study area generally masked the fluctuations that were due to the productivity. The δ44Ca record from the MD81349 core shows that except for special periods like MIS 6.0, most of the calcium isotope oscillation patterns correspond well to variations in productivity. The characteristics of the variations in the substitute proxies, such as the sedimentary flux of the foraminifera as well as δ13C and N. dutertrei, indicate that they significantly affect the formation of the δ44Ca peaks. The Bengal deep-sea fan and the adjacent areas are the centre of terrigenous accumulation in the northern Indian Ocean. According to more than 30 cores from this area, despite the high sedimentary flux during the last glacial maximum, the sedimentary record of fine grains without any coarse sand indicates that the intensity of the terrigenous input is less than that during the other glacial periods that are represented by MIS 4.0 and 6.0. Thus, the productivity effect was clearly reflected in the δ44Ca record. Records of high productivity during MIS 5.0 are rare in the northern Indian Ocean. However, because of rising sea level, the terrigenous input reached the minimum of the 300 ka sedimentary history (Foucault and Fang, 1987), which led to the maximum peak of δ44Ca in that period. However, the maximum interval of δ44Ca does not occur during stage MIS 5.5, when the sea level was the highest and the terrigenous input was the lowest; rather, it lags by more than 10 ka.
We propose two explanations for this. (1) The low δ44Ca values in the seawater due to the strong terrigenous input during MIS 6.0 remained significant during the early part of MIS 5.0. (2) The ubiquitous strong dissolution effect of calcareous shells during the early part of MIS 5.0 in the study area allowed more 40Ca to participate in the sediment-sea water-sediment cycles. The only problem with these explanations is that according to the biogenic fractionation effect, the evolutions of the δ44Ca and δ13C curves should be relatively consistent in terms of reflecting oceanic productivity. However, in MD81349, the δ44Ca variation from 115 to 100 ka is exactly opposite to the δ13C trend. Considering the biological data from this core, δ44Ca reflects the productivity fluctuations during MIS 2.0 to 5.0 even more strongly than δ13C. In other words, the ubiquitous increases in the δ13C values in the northern Indian Ocean at approximately 100 ka do not necessarily indicate significant increases in regional productivity.
5 Conclusions
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(1) The Ca cycle (i.e., the input and output of oceanic calcium) can directly affect the light and heavy Ca isotopic compositions of sea water. This characteristic is easy to observe at high resolution despite the long residence time of calcium in sea water. The fluctuations of δ44Ca in G. sacculifer shells from the MD81349 station at the Nintyeast Ridge are useful for investigating environmental changes over the past 300 ka in the study area.
(2) In the Ca cycle system, the terrigenous input to the ocean is likely to be the key factor that controls the δ44Ca curve. The sedimentary record due to the terrigenous input from the erosion of carbonate rocks in the Himalaya clearly reflects this factor. The terrigenous input to the northeastern Indian Ocean over the past 300 ka is most prominent during MIS 6.0. The characteristics of the δ44Ca variations in the study area provide additional evidence from a new perspective.
(3) Oceanic productivity is also related to the calcium output, which is an important factor for δ44Ca variation in addition to the terrigenous input. While changes in the seawater temperature theoretically and experimentally affect Ca isotopic fractionation, they do not significantly impact the δ44Ca curve due to the synergistic effects of important environmental factors, such as terrigenous input and oceanic productivity output.
Acknowledgements
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The authors are grateful to the laboratory staff, the ship’s crew and the students for making the hard effort to this article. Many thanks to Demo Laboratory, Ctd. MicroMass, for testing δ44Ca.
Funding
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  • The National Programme on Global Change and Air-sea Interaction under contract Nos GASI-03-04-01-03 and GASI-GEOGE-03; the Research Grant of Third Institute of Oceanography, State Oceanic Administration under contract No. 2015015.
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doi: 10.1007/s13131-018-1264-7
  • Receive Date：2017-10-23
  • Online Date：2026-04-14
  • Published：2018-09-25
Article Data
Affiliations
History
  • Received：2017-10-23
  • Accepted：2018-03-23
Funding
The National Programme on Global Change and Air-sea Interaction under contract Nos GASI-03-04-01-03 and GASI-GEOGE-03; the Research Grant of Third Institute of Oceanography, State Oceanic Administration under contract No. 2015015.
Affiliations
    1 Third Institute of Oceanography, State Oceanic Administration, Xiamen 361005, China
    2 Institute of Marine Geology and Geophysics, China University of Geosciences (Beijing), Beijing 100083, China
    3 School of Earth Sciences, China University of Geosciences, Wuhan 430074, China
    4 Demo Laboratory, Ctd. MicroMass, Mantchestt M139PL, United Kingdom
    5 School of Earth Science Environmental Engineering, Anhui University of Science and Technology, Huainan 232001, China
    6 Climate and Environment Sciences Laboratory of the institute Pierre Simon Laplace (LSCE), Gif sur Yvette 75000, France

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表12种不同金属材料的力学参数
科
Family		 属数
Number of
genus		 种数
Number of
species		 占总种数比例
Percentage of
total species (%)		 属
Genus		 种数
Number of
species		 占总种数比例
Percentage of total
species (%)
鹅膏菌科Amanitaceae 2 11 5.26 鹅膏菌属 Amanita 10 4.78
小菇科 Mycenaceae 2 12 5.74 丝盖伞属 Inocybe 5 2.39
多孔菌科 Polyporaceae 8 14 6.70 蜡蘑属 Laccaria 5 2.39
红菇科 Russulaceae 3 23 11.00 小皮伞属 Marasmius 6 2.87
小菇属 Mycena 11 5.26
光柄菇属 Pluteus 5 2.39
红菇属 Russula 17 8.13
栓菌属 Trametes 5 2.39
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