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Volume 30 Issue 2
Apr 2019
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Article Contents
Abstract
0. INTRODUCTION
1. OXYGEN ISOTOPE DATASET
2. METHODS
3. RESULTS
4. DISCUSSION
ACKNOWLEDGMENTS
References
Journal of Earth Science  > 2019  >  30(2): 236-243.
Haijun Song, Paul B. Wignall, Huyue Song, Xu Dai, Daoliang Chu. Seawater Temperature and Dissolved Oxygen over the Past 500 Million Years. Journal of Earth Science, 2019, 30(2): 236-243. doi: 10.1007/s12583-018-1002-2
Citation: Haijun Song, Paul B. Wignall, Huyue Song, Xu Dai, Daoliang Chu. Seawater Temperature and Dissolved Oxygen over the Past 500 Million Years. Journal of Earth Science, 2019, 30(2): 236-243. doi: 10.1007/s12583-018-1002-2
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Seawater Temperature and Dissolved Oxygen over the Past 500 Million Years

doi: 10.1007/s12583-018-1002-2
  • 1.

    State Key Laboratory of Biogeology and Environmental Geology, School of Earth Sciences, China University of Geosciences, Wuhan 430074, China

  • 2.

    School of Earth and Environment, University of Leeds, Leeds LS2 9JT, UK

Funds:

the State Key R & D Project of China 2016YFA0601100

the Biosphere Evolution, Transitions and Resilience Program (BETR) 

the National Natural Science Foundation of China 41821001

the National Natural Science Foundation of China 41661134047

the National Natural Science Foundation of China 41622207

the National Natural Science Foundation of China 41530104

the Natural Environment Research Council's Eco-PT Project NE/P01377224/1

a Marie Curie Fellowship H2020-MSCA-IF-2015-701652

the Strategic Priority Research Program of Chinese Academy of Sciences XDB26000000

More Information
  • Corresponding author: Haijun Song
  • Received Date: 27 Mar 2018
  • Accepted Date: 30 Sep 2018
  • Publish Date: 01 Apr 2019
    Abstract
  • Ocean temperature and dissolved oxygen concentrations are critical factors that control ocean productivity, carbon and nutrient cycles, and marine habitat. However, the evolution of these two factors in the geologic past are still unclear. Here, we use a new oxygen isotope database to establish the sea surface temperature (SST) curve in the past 500 million years. The database is composed of 22 796 oxygen isotope values of phosphatic and calcareous fossils. The result shows two prolonged cooling events happened in the Late Paleozoic and Late Cenozoic, coinciding with two major ice ages indicated by continental glaciation data, and seven global warming events that happened in the Late Cambrian, Silurian- Devonian transition, Late Devonian, Early Triassic, Toarcian, Late Cretaceous, and Paleocene-Eocene transition. The SSTs during these warming periods are about 5-30¦ higher than the present-day level. Oxygen contents of shallow seawater are calculated from temperature, salinity, and atmospheric oxygen. The results show that major dissolved oxygen valleys of surface seawater coincide with global warming events and ocean anoxic events. We propose that the combined effect of temperature and dissolved oxygen account for the long-term evolution of global oceanic redox state during the Phanerozoic.

     

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  • Global warming is becoming a major environmental problem for humans in the twenty-first century. Global mean surface air temperature rose ~1 ℃ in the past century and it is likely that they will rise by > 1 ℃ toward the end of this century (Brown and Caldeira, 2017; Meinshausen et al., 2009). Rising ocean temperatures have profound impacts on reef ecosystems, triggering mass bleaching of corals (Hughes et al., 2017). Potentially severe consequences of global warming include the declines in dissolved oxygen (DO) in the ocean interior and an expansion in the area and volume of oceanic oxygen minimum zones (Stramma et al., 2008), which may further lead to significant changes in biogeochemical cycles and mass extinctions for marine organisms.

    Ocean temperature and DO concentrations have varied greatly in the geologic time. For example, sea surface temperature (SST) rose 4–8 ℃ within a few thousand years at the Paleocene-Eocene transition about 55 Ma, which was accompanied by enhanced seawater anoxia and extinctions of benthic foraminifers (Dickson et al., 2012; Zachos et al., 2003, Kennett and Stott, 1991). The rapid warming of ~10 ℃ at the Permian-Triassic transition about 252 Ma is probably the most conspicuous example (Joachimski et al., 2012; Sun et al., 2012). The temperature rise and associated widespread oceanic anoxia are likely the main killing mechanism for the most severe extinction of marine organisms in the Phanerozoic Eon (Penn et al., 2018; Song et al., 2014).

    The SST of ancient oceans is mainly assessed using oxygen isotope values from fossil shells. A critical issue for oxygen isotope paleothermometry is the uncertainty of the composition of seawater δ18O in deep time, whether it remained constant or changed significantly. Previous SST estimates in the Phanerozoic usually used an increased seawater δ18O with ~1‰ per 108 years (Veizer and Prokoph, 2015; Veizer et al., 2000). In this scenario, the resulting SST curve cannot explain the two first-grade cooling events in the Early Paleozoic and Middle Mesozoic because robust glacial evidence is lacking (Royer et al., 2004). Additionally, the cold climates in the Early Paleozoic conflict with extreme high level of atmospheric CO2 derived from the GEOCARBSULF model (Royer et al., 2014; Berner, 2006) and multiple proxies (Foster et al., 2017). Furthermore, recent clumped isotope evidence shows that the composition of seawater δ18O is almost invariant over the past 500 million years (Henkes et al., 2018). Here, we have assumed an invariant oxygen isotope composition of seawater to calculate temperatures in deep time.

    Oxygen isotope measurements of carbonate fossils are useful in reconstructing ancient SSTs in the younger Cenozoic and Mesozoic eras, but commonly yield questionable results for the Paleozoic Era (Veizer and Prokoph, 2015; Grossman, 2012). Paleozoic δ18O values from brachiopods show an extremely wide range in composition from ~0‰ to -10‰ and, if the values are primary, then the calculated temperatures are unrealistically high, reaching 70 ℃ in the Early Paleozoic (Grossman, 2012). One scenario is that the older the samples are, the more likely the δ18O values from these samples are diagenetically altered (Grossman et al., 1996). Recent studies have shown that phosphate fossils (e.g., conodont) are more reliable records of original seawater oxygen isotopes than biogenic carbonates (Trotter et al., 2008; Joachimski et al., 2004). Thousands of oxygen isotope measurements on Paleozoic and Triassic conodonts have been published in the past decades. These results, combined with numerous data from the Mesozoic and Cenozoic carbonate fossils, make it possible to establish a reliable SST curve for the past 500 million years.

    There is no means to directly measure seawater oxygen content of ancient oceans. The primary source of DO in surface seawater is air-sea exchange with atmospheric O2, leading to approximate saturation. Therefore, the DO of surface seawater relies principally on atmospheric oxygen content, SST and salinity. A reliable O2 curve for Phanerozoic atmosphere has been estimated by using the GEOCARBSULF model (Royer et al., 2014; Berner, 2006). In addition, the salinity changes of the oceans during the Phanerozoic have been constructed by a compiled dataset of volumes and masses of evaporate deposits (Hay et al., 2006). Thus, the evolution of seawater oxygen content in the geologic past can be assessed from estimated atmospheric O2 and ocean salinity, and temperature that we constructed based on oxygen isotopes.

    A total of 22 796 oxygen isotope measurements of carbonate/phosphate fossils are selected to establish SST curve over the past 500 million years (see Fig. 1 and Daraset S1). The dataset is composed of published δ18O measurements. A total of 8 782 δ18O measurements are from the Phanerozoic database of Veizer and Prokoph (2015), 3 383 measurements are from Phanerozoic database of Grossman (2012), 1 677 measurements are from Cretaceous database of O'Brien et al. (2017), and 161 measurements are from Jurassic database of Dera et al. (2011). The other 8 793 δ18O measurements have been compiled in this study. A total of 3 643 δ18O measurements are from phosphate fossils, including phosphatic brachiopods (46), conodonts (3 299), and fishes (298), while 19 153 δ18O measurements are from carbonate fossils, including belemnites (1 663), bivalves (720), brachiopods (574), benthic foraminifers (129), planktonic foraminifers (15 500), gastropods (179), and coccoliths (388).

    Figure  1.  Raw oxygen isotope data used for reconstructing sea surface temperatures over the past 500 million years. A total of 22 796 oxygen isotopic measurements are used (see Dataset S1). The scale of δ18OPhos is used for phosphatic fossils including phosphatic brachiopod, conodont, and fish. The scale of δ18OCarb is used for carbonate fossils including belemnite, bivalve, brachiopod, planktonic foraminifer, and others. The scale of temperature is used for all fossils. Dark red short line: phosphatic brachiopod; purple plus sign: conodont; red diamond: fish; blue circle: belemnite; dark red triangle: bivalve; green star: brachiopod; blue multiple sign: planktonic foraminifer; orange square: other carbonate fossils
    DownLoad: Full-Size Img PowerPoint

    Not all data are used to reconstructing the SST curve. The selection of data depends mainly on the following three principles. First, only data from marine fossils that represent organisms living in the shallow water habitats are selected, i.e., shallow planktons (planktonic foraminifers), nektons (conodonts, fishes, and belemnites), and benthos (bivalves, brachiopods, and gastropods), but the bathyal benthic foraminifers are excluded. Second, only lower-paleolatitude data (between 40°N and 40°S) from well-preserved specimens are selected. Not only because δ18O data from lower-paleolatitudes are abundant but also because of the strong temperature gradient between the equator and polar regions. For the regions between 40°N and 40°S, the latitude thermal gradient was much weaker under both present-day cool and Late Cretaceous warm climates (Sinninghe Damsté et al., 2010). Third, only δ18O from phosphate fossils are selected for the Paleozoic Era because of the unreliability of δ18O from carbonate fossils of this age. δ18O from carbonate fossils have a great range in composition and the significant positive correlation with δ13C (n = 4 532, r = 0.64, p < 0.001, Fig. 2a), suggesting these data are probably affected by diagenetic alteration. However, there is no δ13C-δ18O covariance for the Mesozoic and Cenozoic carbonate fossils (n = 2 066, r = 0.03, p = 0.171, Fig. 2b). Therefore, Mesozoic and Cenozoic δ18O are compiled from both carbonate and phosphate fossils.

    Figure  2.  Cross plots of carbon and oxygen isotopes of carbonate fossils from Phanerozoic. (a) Cross plot of Paleozoic δ13C versus δ18O showing a clear positive relationship (n = 4 532, r = 0.64, p < 0.001). (b) Mesozoic and Cenozoic δ13C versus δ18O. There is no δ13C-δ18O covariance for the entire data (n = 2 066, r = 0.03, p = 0.171). Data from Grossman (2012)
    DownLoad: Full-Size Img PowerPoint

    2.1 Paleo-Sea Surface Temperature Assessment from δ18O Dataset

    Phosphate δ18O values were converted to seawater temperatures by using the equation of Lécuyer et al. (2013), assuming an average δ18O value of the ocean of -1‰

    t=117.4−4.5×(δ18OPO4−δ18OSW)×1000

    where t is the sea surface temperature (℃), δ18OPO4 is the O isotope composition of phosphate fossils (‰, VSMOW); δ18OSW is the O isotope composition of seawater (‰, VSMOW).

    Seawater temperatures were calculated from the carbonate δ18O by using equation of Hays and Grossman (1991)

    t=15.7−4.36×(δ18OCarb−δ18OSW)×1000+0.12×[(δ18OCarb−δ18OSW)×1000]2

    where δ18OCarb is the O isotope composition of carbonate fossils (‰, VPDB).

    2.2 Dissolved Oxygen of Shallow Oceans

    The solubility equation for oxygen is based on equation of Benson and Krause (1984)

    DO=O2[F(1−Pwv)(1−θo)ko,sMw]
    F=1000−0.716582×S
    Pwv=108.07131−1730.63/(233.426+t)/760
    (1−θo)=0.999025+1.426×10−5t−6.436×10−8t2
    ko,s=e3.71814+5596.17/T−1049668/T2+S(0.0225034−13.6083/T+2565.68/T2)

    where DO is the standard air solubility concentrations of oxygen (mol/kg); O2 is the atmospheric oxygen concentration; F is a salinity factor; S is the salinity of seawater (g/kg); Pwv is vapor pressure of water (atm); θo is a constant that depends on the second virial coefficient of oxygen; ko, s is Henry coefficient for oxygen (atm); Mw is mean molecular mass of sea salt (18.015 3 g/mol); t is temperature in degrees Celsius (℃); T = temperature in kelvins (K).

    2.3 Dissolved Oxygen of Deep Oceans

    Deep ocean oxygen is calculated by using the equation of Sarmiento et al. (1988)

    DOd=DOh−r(PO4d−PO4h)
    PO4h=PO4dfhd−Phfhd+T

    where DOd is the dissolved oxygen of deep oceans; DOh is the dissolved oxygen of high-latitude surface oceans; r is the Redfield ratio of oxygen consumption to phosphate production accompanying the oxidation of organic matter (r = ~169 for present ocean). PO4d is the phosphate concentration of deep oceans; PO4h is the phosphate concentration of high-latitude surface oceans; fhd is a circulation parameter representing local convective overturning in deep water formation regions (fhd = ~45×106 m3/s for present ocean). Ph is the particulate rain of phosphate from the high-latitude deep water formation regions (Ph = 2.31×106 mol C/s for present ocean). T is the large-scale thermohaline overturning (T = ~19×106 m3/s for present ocean).

    3.1 Estimating Seawater Temperature

    Oxygen isotope data from carbonate and phosphate fossils provide a Late Cambrian to present SST curve (Fig. 3). These temperature estimates exhibit first-order variations characterized by warm climate in the Early Paleozoic–Devonian and Mesozoic–Early Cenozoic, and cool climate in the Late Paleozoic and Late Cenozoic. The Late Cambrian saw the warmest climate of the past 500 million years with SST reaching to ~45 ℃. Although a rapid cooling occurred in the Late Cambrian–Early Ordovician, the SST of the Ordovician, Silurian, and Devonian is maintained at a high level around 30 ℃. Another warm period occurred in the Mesozoic–Early Cenozoic, during which the SST fluctuated around 22 ℃. Two cool intervals are identified in the Late Paleozoic and Late Cenozoic, respectively. Seawater temperature during these two cool intervals fluctuated around 17 ℃ and has a lowest level of 12 ℃ in the Late Carboniferous.

    Figure  3.  Low-latitude sea surface temperatures, continental-scale ice sheets, and CO2 concentrations for the past 500 million years. Each temperature dot presents the mean value per one million years (data see Table S1). Vertical error bars show 95% confidence intervals. The smoothed curve is locally weighted linear regressions (LOWESS, red line). Glaciological data for ice sheets are modified from (Crowley and Berner, 2001). Atmospheric CO2 concentrations are from the GEOCARBSULF model (orange dash line) (Royer et al., 2014) and multiple proxies (orange solid line) (Foster et al., 2017). Global warming events (GWEs) are peaks identified from the temperature curve. The peak the Late Carboniferous is not considered as a GWE because the maximum temperature during this interval is only ~20 ℃, which is lower than most of Phanerozoic temperatures. LC. Late Cambrian; SD. Silurian–Devonian; FF. Frasnian–Famennian; ET. Early Triassic; TO. Toarcian; LK. Late Cretaceous; PE. Paleocene–Eocene
    DownLoad: Full-Size Img PowerPoint

    The second-order variations of temperatures derived from fossil oxygen isotopes reveal seven global warming events (GWEs): in the Late Cambrian, Silurian–Devonian transition, Frasnian–Famennian transition, Early Triassic, Toarcian, Late Cretaceous, and Paleocene–Eocene transition (Fig. 3). The SSTs in the global warming intervals were significantly higher than present-day average temperatures, and witnessed a downward trend to younger intervals (Fig. 3). The SSTs during the Paleocene–Eocene GWE and Mesozoic GWEs are about 5 and 10 ℃ higher than the present-day level, respectively. However, the SSTs in the Late Cambrian and the Early and Late Devonian look extraordinarily high, about 30 and 15 ℃ higher than the present level, respectively.

    3.2 Estimating Dissolved Oxygen of Shallow Seawater

    Dissolved oxygen of oceans is influenced by many factors such as atmospheric oxygen level, temperature, organic productivity, and ocean currents (Sarmiento et al., 1988). However, for the surface seawater, it mainly depends on the former two because seawater oxygen dominantly comes from atmosphere by air-sea exchanging process. Marine primary producers generate and release a large amount of oxygen in the photic zones through photosynthesis. However, most of the oxygen escapes into the atmosphere within a short time because the surface seawater is near-saturated with oxygen. Therefore, the DO in the surface seawater depends primarily on factors that control the saturation of oxygen in seawaters such as temperature, atmospheric oxygen level, and salinity. The DO of surface seawater has a positive relationship with atmospheric oxygen level, but a negative relationship with temperature and salinity (Figs. 4a, 4b).

    Figure  4.  The relationship between seawater oxygen concentration and impact factors in the oceans. (a) Surface seawater oxygen concentration versus temperature (at salinity = 35‰). (b) Surface seawater oxygen concentration versus salinity (at temperature = 25 ℃). (c) Deep-water oxygen concentration versus rate of deep-water formation (represented by fhd). (d) Deep-water oxygen concentration versus phosphorus availability (represented by PO4d–PO4h). The calculations in c and d are done at present-ocean conditions, i.e., Ph = 2.31×106 mol C/s, r = 169, T = 19×106 m3/s, DOh = 325 μM, and PO4d = 2.15 μM (Sarmiento et al., 1988). POL, present oceanic level of dissolved oxygen. POL of high-latitude surface seawater is 325 μM (Sarmiento et al., 1988)
    DownLoad: Full-Size Img PowerPoint

    Surface seawater oxygen concentrations in the ancient near-tropic oceans are calculated based on the solubility equation for oxygen by using published salinity (Hay et al., 2006), atmospheric O2 (Royer et al., 2014), and the estimated temperature curve in this study (see Section 2). The result shows four major DO peaks in the Late Ordovician–Early Devonian (~250 μM), Late Paleozoic (~350 μM), Middle–Late Triassic (~250 μM), and Cretaceous–Cenozoic (~270 μM), and four major valleys in the Late Cambrian–Early Ordovician (~110 μM), Late Devonian (~130 μM), Early Triassic (~170 μM), and Early Jurassic (~110 μM) (Fig. 5).

    Figure  5.  Dissolved oxygen, sea surface temperature and oceanic anoxic events for the past 500 million years. Dissolved oxygen values are calculated from temperature, atmospheric oxygen, and salinity. The temperature curve is from Fig. 2. The shade shows 90% confidence interval. Oceanic anoxic events (OAEs) are compiled based on Table S2. LC. Late Cambrian; FF. Frasnian–Famennian; ET. Early Triassic; HS. Hettangian–Sinemurian; TO. Toarcian; K. Cretaceous; PE. Paleocene–Eocene
    DownLoad: Full-Size Img PowerPoint

    4.1 The Reliability of Established Temperature Curve

    There are still many uncertainties about reconstructing temperatures of ancient oceans. The critical issue is the composition of seawater oxygen isotope that we have discussed above. The second issue is the diverse habitats of different fossil groups. Although marine animals that were used to calculating temperature are shallow dwellers, most of them have a wide habitat in depth from 0 to 100–200 m. Therefore, the estimated temperature is a mixture of values from shelf waters. The third issue is seawater pH. Changes in seawater pH normally result in oxygen isotope incorporation in carbonates and produce bias on δ18O-derived temperatures (Royer et al., 2004). However, oxygen isotopes from carbonate fossils are mainly from the post-Triassic interval when there was much less ${p_{CO}}_{_2}$ variation than in the Paleozoic (Foster et al., 2017; Royer et al., 2014). In addition, other factors such as icehouse climate and diagenesis could also potentially affect the accuracy of oxygen isotope paleothermometry (Grossman, 2012). For the temperature values calculated based on raw oxygen isotope data from different fossil groups, although some data deviate from the trend, the overall change is consistent (Figs. 1, 3), suggesting the established SST curve is reliable.

    4.2 The Reliability of Established Dissolved Oxygen Curve

    A critical limitation when reconstructing the oxygen content of surface seawater is the uncertain of paleo-O2 and salinity. Atmospheric O2 in geologic time is usually reconstructed through geochemical models, i.e., GEOCARB-style models (Krause et al., 2018; Royer et al., 2014; Berner, 2006; Falkowski et al., 2005; Bergman, 2004). However, these constructions are only moderately constrained by proxies. Charcoal is a product of wildfire that occurs when oxygen content is over 15% (Belcher and McElwain, 2008). Sedimentary records show that charcoal is present in the sedimentary rocks of the past 400 Ma (Glasspool and Scott, 2010), suggesting oxygen content over 15% for much of the Phanerozoic. This observation is in keeping with geochemical models except in the Jurassic interval (Belcher and McElwain, 2008). Another limitation of reconstruction of seawater oxygen content is that paleo-salinity records are uncertain for the limited knowledge of the history of water on Earth. However, salinity of the past 500 million years was likely within a narrow range of between 30‰ and 50‰ (Hay et al., 2006). In this range, salinity only has a small contribution to the uncertainty of reconstruction of DO content (Fig. 4b).

    4.3 The Possible Drivers of Phanerozoic Temperature Change

    The first-order temperature variations are supported by robust and independent glaciological data for continental-scale ice sheets (Crowley and Berner, 2001) and carbonate clumped isotope data of fossil brachiopod and mollusk shells (Henkes et al., 2018; Came et al., 2007). For instance, the two major intervals of continental glaciation from the Late Paleozoic (ca. 338–256 Ma) and Late Cenozoic (ca. 40–0 Ma) (Crowley and Berner, 2001) coincide closely with the two lowest-temperature intervals in the past 500 Ma (Figs. 1, 3). The transition from Early Paleozoic warm climate to Late Paleozoic cool climate can be also reflected in the carbonate-clumped isotopes (Henkes et al., 2018). The estimated SST curve shows that the Late Paleozoic ice age witnessed the coldest climate over the past 500 Ma. The lowest temperature of shallow seawater during the Late Paleozoic is about 5 ℃ lower than the present-day level, which is in accord with the glaciological evidence that shows the longest and largest glacial period of the Phanerozoic at this time (Fielding et al., 2008).

    Independent evidence is available for many of the second-order variations of temperatures. For example, the Paleocene-Eocene thermal maximum, PETM has been identified using multiple proxies in addition to oxygen isotope including foraminiferal magnesium/calcium ratios (Tripati and Elderfield, 2005) and TEX86 derived from the membrane lipids of marine picoplankton (Sluijs et al., 2006; Zachos et al., 2006). Toarcian GWE is independently supported by the abrupt increase of atmospheric CO2 obtained from fossil leaf stomatal frequency (McElwain et al., 2005). Early Triassic GWE reflected by marine conodont O isotopes coincided with the elevated air temperatures recorded by O isotopes from continental tetrapods (Rey et al., 2016).

    Atmospheric CO2 concentrations from the GEOCARBSULF model show a strong positive correlation between SST and CO2 (r = 0.853, n = 51, p < < 0.001, see Fig. 6 and Table S2). Warm periods are characterized by higher CO2 horizons, i.e., Early Paleozoic, Mesozoic, and Early Cenozoic. Cool periods are marked by lower CO2 horizons such as Late Paleozoic and Late Cenozoic. However, the latest Ordovician ice age is an exception. Although temperature in this interval is the lowest of the Ordovician (Figs. 1, 3), CO2 is at a high level of ~2 500 ppm (Royer et al., 2014). It might be because the duration of the latest Ordovician glaciation was very short (~1 million years) (Finnegan et al., 2011), but the GEOCARBSULF model generally has a time-step of 10 million years (Royer et al., 2014). The overall striking correspondence between CO2 concentrations and surface temperatures supports the proposal that high CO2 concentrations drive or amplify high global temperatures (Berner, 2001; Crowley and Berner, 2001).

    Figure  6.  Cross plots of sea surface temperature and atmospheric carbon dioxide (r = 0.853, n = 51, p < 0.001; Table S3). The shade shows 95% confidence interval. Atmospheric CO2 concentrations are from the GEOCARBSULF model (Royer et al., 2014)
    DownLoad: Full-Size Img PowerPoint

    In addition, temperature evolution calculated by oxygen isotope data seems to be associated with galactic cosmic ray flux (Shaviv and Veizer, 2003). In principle, the variations of cosmic ray flux likely contribute to the temperature evolution via controlling the formation of clouds at low latitudes (Shaviv and Veizer, 2003). Cold ages in the Late Paleozoic and Late Cenozoic coincide with high cosmic ray fluxes, whereas most warm climate intervals are characterized by low cosmic ray fluxes, e.g., Cambrian, Devonian, Triassic and Cretaceous. Only the Mid-Jurassic warm period is an exception because it occurs during a time of low cosmic ray level (Shaviv and Veizer, 2003).

    4.4 The Drivers of Phanerozoic Ocean Redox State

    The DO curve shows similar features of atmospheric O2 derived from Geocarbsulf model (Royer et al., 2014; Berner, 2006), suggesting atmospheric O2 level is a major factor controlling long-term evolution of oxygen content of surface seawater. The second-order variations are associated intimately with temperature, e.g., valleys of DO closely coincide with global warming events (see Fig. 5).

    The reconstructed DO curve is supported by independent data on oceanic anoxic events (OAEs). Sedimentary and geochemical data show at least nine OAE intervals in the past 500 million years, i.e., Late Cambrian, Frasnian–Famennian transition, Early Triassic, Hettangian–Sinemurian, Toarcian, Aptian–Albian, Cenomanian–Turonian, Coniacian–Santonian, and Paleocene–Eocene transition (Song et al., 2017; Meyer and Kump, 2008, and Table S3). Most of those OAEs coincide with low levels of DO, especially the very low levels (<150 μM) seen in the Late Cambrian, Late Devonian, and Early Jurassic (Fig. 5). Additionally, OAEs show good correspondence with global warming events. Under a warm climate, surface seawaters absorb less oxygen, but probably also important is the likelihood of less efficient ocean circulation at these times (Sarmiento et al., 1988). Temperature is a major contributing factor on the rate of formation of deep water (fhd) by controlling the strength of ocean thermohaline circulation. In modern oceans, fhd is positively correlated with deep seawater oxygen (Fig. 4c). Therefore, deep ocean anoxia usually appeared under low fhd associated with global warming events.

    Oxygen content of surface seawater is a significant factor affecting the redox state of deep oceans. When surface DO is up to 1.5 times of present-level, it is difficult to cause deep-water anoxia even under low fhd (Fig. 4c). Conversely, when surface DO fall to half, it can easily lead to anoxia in deep oceans. Another essential factor controlling the redox state of deep ocean is nutrient availability (represented by PO4d–PO4h) (Sarmiento et al., 1988), which has a negative relationship with deep seawater oxygen content (Fig. 4d). Some OAEs occurred in the periods of high surface DO levels, such as Cretaceous OAE1, 2, and 3, and Paleocene–Eocene OAE. High temperatures might be the most important factor for these OAEs by reducing the the solubility of oxygen and producing sluggish ocean circulations. In addition, global warming was usually accompanied by enhanced continental weathering and increased nutrient input to oceans (Jenkyns, 2010), which would further increase the rate of oxygen consumption and lead to a global OAE faster.

    We thank Zhipu Qiu for collecting data, Ján Veizer for comments on earlier drafts, and Dana L. Royer for providing atmospheric oxygen and carbon dioxide data. This study is supported by the National Natural Science Foundation of China (Nos. 41821001, 41622207, 41530104, 41661134047), the State Key R & D Project of China (No. 2016YFA0601100), and the Strategic Priority Research Program of Chinese Academy of Sciences (No. XDB26000000), a Marie Curie Fellowship (No. H2020-MSCA-IF-2015-701652), and the Natural Environment Research Council's Eco-PT Project (No. NE/P01377224/1), which is a part of the Biosphere Evolution, Transitions and Resilience Program (BETR). The final publication is available at Springer via https://doi.org/10.1007/s12583-018-1002-2.

    Electronic Supplementary Materials: Supplementary materi-als (Dataset S1, Tables S1, S2, S3) are available in the online version of this article at https://doi.org/10.1007/s12583-018-1002-2.

    • References(49)
  • Belcher, C. M., McElwain, J. C., 2008. Limits for Combustion in Low O2 Redefine Paleoatmospheric Predictions for the Mesozoic. Science, 321(5893):1197-1200. https://doi.org/10.1126/science.1160978
    Benson, B. B., Krause, D. Jr., 1984. The Concentration and Isotopic Frac-tionation of Oxygen Dissolved in Freshwater and Seawater in Equilib-rium with the Atmosphere1. Limnology and Oceanography, 29(3):620-632. https://doi.org/10.4319/lo.1984.29.3.0620
    Bergman, N. M., 2004. COPSE:A New Model of Biogeochemical Cycling over Phanerozoic Time. American Journal of Science, 304(5):397-437. https://doi.org/10.2475/ajs.304.5.397
    Berner, R. A., 2001. GEOCARB Ⅲ:A Revised Model of Atmospheric CO2 over Phanerozoic Time. American Journal of Science, 301(2):182-204. https://doi.org/10.2475/ajs.301.2.182
    Berner, R. A., 2006. GEOCARBSULF:A Combined Model for Phanerozoic Atmospheric O2 and CO2. Geochimica et Cosmochimica Acta, 70(23):5653-5664. https://doi.org/10.1016/j.gca.2005.11.032
    Brown, P. T., Caldeira, K., 2017. Greater Future Global Warming Inferred from Earth's Recent Energy Budget. Nature, 552(7683):45-50. https://doi.org/10.1038/nature24672
    Came, R. E., Eiler, J. M., Veizer, J., et al., 2007. Coupling of Surface Temperatures and Atmospheric CO2 Concentrations during the Palaeozoic Era. Nature, 449(7159):198-201. https://doi.org/10.1038/nature06085
    Crowley, J. K., Berner, R. A., 2001. CO2 and Climate Change. Science, 292:870-872. https://doi.org/10.1126/science.1061664
    Dera, G., Brigaud, B., Monna, F., et al., 2011. Climatic Ups and Downs in a Disturbed Jurassic World. Geology, 39(3):215-218. https://doi.org/10.1130/g31579.1
    Dickson, A. J., Cohen, A. S., Coe, A. L., 2012. Seawater Oxygenation during the Paleocene-Eocene Thermal Maximum. Geology, 40(7):639-642. https://doi.org/10.1130/g32977.1
    Falkowski, P. G., Katz, M. E., Milligan, A. J., et al., 2005. The Rise of Oxygen over the Past 205 Million Years and the Evolution of Large Placental Mammals. Science, 309(5744):2202-2204. https://doi.org/10.1126/science.1116047
    Fielding, C. R., Frank, T. D., Isbell, J. L., 2008. The Late Paleozoic Ice Age-A Review of Current Understanding and Synthesis of Global Climate Patterns. In: Fielding, C. R., Frank, T. D., Isbell, J. L., eds., Resolving the Late Paleozoic Ice Age in Time and Space, 441: 343-354
    Finnegan, S., Bergmann, K., Eiler, J. M., et al., 2011. The Magnitude and Duration of Late Ordovician-Early Silurian Glaciation. Science, 331(6019):903-906. https://doi.org/10.1126/science.1200803
    Foster, G. L., Royer, D. L., Lunt, D. J., 2017. Future Climate Forcing Potentially without Precedent in the Last 420 Million Years. Nature Communications, 8:14845. https://doi.org/10.1038/ncomms14845
    Glasspool, I. J., Scott, A. C., 2010. Phanerozoic Concentrations of Atmos-pheric Oxygen Reconstructed from Sedimentary Charcoal. Nature Ge-oscience, 3(9):627-630. https://doi.org/10.1038/ngeo923
    Grossman, E. L., Mii, H. S., Zhang, C. L., et al., 1996. Chemical Variation in Pennsylvanian Brachiopod Shells-Diagenetic, Taxonomic, Micro-structural, and Seasonal Effects. SEPM Journal of Sedimentary Research, 66(5):1011-1022. https://doi.org/10.1306/d4268469-2b26-11d7-8648000102c1865d
    Grossman, E. L., 2012. Oxygen Isotope Stratigraphy. In: Gradstein, F. M., Ogg, J. G., Schmitz, M. D., et al., eds., The Geologic Time Scale 2012. Elsevier. 195-220
    Hay, W. W., Migdisov, A., Balukhovsky, A. N., et al., 2006. Evaporites and the Salinity of the Ocean during the Phanerozoic:Implications for Climate, Ocean Circulation and Life. Palaeogeography, Palaeoclimatology, Palaeoecology, 240(1/2):3-46. https://doi.org/10.1016/j.palaeo.2006.03.044
    Hays, P. D., Grossman, E. L., 1991. Oxygen Isotopes in Meteoric Calcite Cements as Indicators of Continental Paleoclimate. Geology, 19(5):441. https://doi.org/10.1130/0091-7613(1991)019<0441:oiimcc>2.3.co;2 doi: 10.1130/0091-7613(1991)019<0441:oiimcc>2.3.co;2
    Henkes, G. A., Passey, B. H., Grossman, E. L., et al., 2018. Temperature Evolution and the Oxygen Isotope Composition of Phanerozoic Oceans from Carbonate Clumped Isotope Thermometry. Earth and Planetary Science Letters, 490:40-50. https://doi.org/10.1016/j.epsl.2018.02.001
    Hughes, T. P., Kerry, J. T., Álvarez-Noriega, M., et al., 2017. Global Warming and Recurrent Mass Bleaching of Corals. Nature, 543(7645):373-377. https://doi.org/10.1038/nature21707
    Jenkyns, H. C., 2010. Geochemistry of Oceanic Anoxic Events. Geochemis-try, Geophysics, Geosystems, 11(3):Q03004. https://doi.org/10.1029/2009gc002788
    Joachimski, M. M., van Geldern, R., Breisig, S., et al., 2004. Oxygen Isotope Evolution of Biogenic Calcite and Apatite during the Middle and Late Devonian. International Journal of Earth Sciences, 93(4):542-553. https://doi.org/10.1007/s00531-004-0405-8
    Joachimski, M. M., Lai, X., Shen, S., et al., 2012. Climate Warming in the Latest Permian and the Permian-Triassic Mass Extinction. Geology, 40(3):195-198. https://doi.org/10.1130/g32707.1
    Kennett, J. P., Stott, L. D., 1991. Abrupt Deep-Sea Warming, Palaeoceano-graphic Changes and Benthic Extinctions at the End of the Palaeocene. Nature, 353(6341):225-229. https://doi.org/10.1038/353225a0
    Krause, A. J., Mills, B. J. W., Zhang, S., et al., 2018. Stepwise Oxygenation of the Paleozoic Atmosphere. Nature Communications, 9(1):4081. https://doi.org/10.1038/s41467-018-06383-y
    Lécuyer, C., Amiot, R., Touzeau, A., et al., 2013. Calibration of the Phos-phate δ18O Thermometer with Carbonate-Water Oxygen Isotope Frac-tionation Equations. Chemical Geology, 347:217-226. https://doi.org/10.13039/501100004794
    McElwain, J. C., Wade-Murphy, J., Hesselbo, S. P., 2005. Changes in Carbon Dioxide during an Oceanic Anoxic Event Linked to Intrusion into Gondwana Coals. Nature, 435(7041):479-482. https://doi.org/10.1038/nature03618
    Meinshausen, M., Meinshausen, N., Hare, W., et al., 2009. Greenhouse-Gas Emission Targets for Limiting Global Warming to 2℃. Nature, 458(7242):1158-1162. https://doi.org/10.1038/nature08017
    Meyer, K. M., Kump, L. R., 2008. Oceanic Euxinia in Earth History:Causes and Consequences. Annual Review of Earth and Planetary Sciences, 36(1):251-288. https://doi.org/10.1146/annurev.earth.36.031207.124256
    O'Brien, C. L., Robinson, S. A., Pancost, R. D., et al., 2017. Cretaceous Sea-Surface Temperature Evolution:Constraints from TEX 86 and Planktonic Foraminiferal Oxygen Isotopes. Earth-Science Reviews, 172:224-247. https://doi.org/10.1016/j.earscirev.2017.07.012
    Penn, J. L., Deutsch, C., Payne, J. L., et al., 2018. Temperature-Dependent Hypoxia Explains Biogeography and Severity of End-Permian Marine Mass Extinction. Science, 362(6419):eaat1327. https://doi.org/10.1126/science.aat1327
    Rey, K., Amiot, R., Fourel, F., et al., 2016. Global Climate Perturbations during the Permo-Triassic Mass Extinctions Recorded by Continental Tetrapods from South Africa. Gondwana Research, 37:384-396. https://doi.org/10.1016/j.gr.2015.09.008
    Royer, D. L., Berner, R. A., Montañez, I. P., et al., 2004. CO2 as a Primary Driver of Phanerozoic Climate. GSA Today, 14(3):3-7. https://doi.org/10.1130/1052-5173(2004)014<4:caapdo>2.0.co;2 doi: 10.1130/1052-5173(2004)014<4:caapdo>2.0.co;2
    Royer, D. L., Donnadieu, Y., Park, J., et al., 2014. Error Analysis of CO2 and O2 Estimates from the Long-Term Geochemical Model GEOCARB-SULF. American Journal of Science, 314(9):1259-1283. https://doi.org/10.2475/09.2014.01
    Sarmiento, J. L., Herbert, T. D., Toggweiler, J. R., 1988. Causes of Anoxia in the World Ocean. Global Biogeochemical Cycles, 2(2):115-128. https://doi.org/10.1029/gb002i002p00115
    Shaviv, N. J., Veizer, J., 2003. Celestial Driver of Phanerozoic Climate?. GSA Today, 13(7):4-10. https://doi.org/10.1130/1052-5173(2003)013<0004:cdopc>2.0.co;2 doi: 10.1130/1052-5173(2003)013<0004:cdopc>2.0.co;2
    Sinninghe Damsté, J. S., van Bentum, E. C., Reichart, G. J., et al., 2010. A CO2 Decrease-Driven Cooling and Increased Latitudinal Temperature Gradient during the Mid-Cretaceous Oceanic Anoxic Event 2. Earth and Planetary Science Letters, 293(1/2):97-103. https://doi.org/10.1016/j.epsl.2010.02.027
    Sluijs, A., Schouten, S., Pagani, M., et al., 2006. Subtropical Arctic Ocean Temperatures during the Palaeocene/Eocene Thermal Maximum. Nature, 441(7093):610-613. https://doi.org/10.1038/nature04668
    Song, H. J., Wignall, P. B., Chu, D. L., et al., 2014. Anoxia/High Temperature Double Whammy during the Permian-Triassic Marine Crisis and Its Aftermath. Scientific Reports, 4(1):4132. https://doi.org/10.1038/srep04132
    Song, H. J., Jiang, G. Q., Poulton, S. W., et al., 2017. The Onset of Wide-spread Marine Red Beds and the Evolution of Ferruginous Oceans. Na-ture Communications, 8(1):399. https://doi.org/10.1038/s41467-017-00502-x
    Stramma, L., Johnson, G. C., Sprintall, J., et al., 2008. Expanding Oxy-gen-Minimum Zones in the Tropical Oceans. Science, 320(5876):655-658. https://doi.org/10.1126/science.1153847
    Sun, Y., Joachimski, M. M., Wignall, P. B., et al., 2012. Lethally Hot Temperatures during the Early Triassic Greenhouse. Science, 338(6105):366-370. https://doi.org/10.1126/science.1224126
    Tripati, A., Elderfield, H., 2005. Deep-Sea Temperature and Circulation Changes at the Paleocene-Eocene Thermal Maximum. Science, 308(5730):1894-1898. https://doi.org/10.1126/science.1109202
    Trotter, J. A., Williams, I. S., Barnes, C. R., et al., 2008. Did Cooling Oceans Trigger Ordovician Biodiversification? Evidence from Conodont Thermometry. Science, 321(5888):550-554. https://doi.org/10.1126/science.1155814
    Veizer, J., Godderis, Y., François, L. M., 2000. Evidence for Decoupling of Atmospheric CO2 and Global Climate during the Phanerozoic Eon. Nature, 408(6813):698-701. https://doi.org/10.1038/35047044
    Veizer, J., Prokoph, A., 2015. Temperatures and Oxygen Isotopic Composi-tion of Phanerozoic Oceans. Earth-Science Reviews, 146:92-104. https://doi.org/10.1016/j.earscirev.2015.03.008
    Zachos, J. C., Wara, M. W., Bohaty, S., et al., 2003. A Transient Rise in Tropical Sea Surface Temperature during the Paleocene-Eocene Thermal Maximum. Science, 302(5650):1551-1554. https://doi.org/10.1126/science.1090110
    Zachos, J. C., Schouten, S., Bohaty, S., et al., 2006. Extreme Warming of Mid-Latitude Coastal Ocean during the Paleocene-Eocene Thermal Maximum:Inferences from TEX86 and Isotope Data. Geology, 34(9):737-740. https://doi.org/10.1130/g22522.1
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    1. Chang Lu, Miao-Qin Lin, Jun Shen, et al. A continental record of Early Cretaceous (Aptian) vegetation and climate change based on palynology and clay mineralogy from the North China Craton. Palaeogeography, Palaeoclimatology, Palaeoecology, 2025, 662: 112750. doi:10.1016/j.palaeo.2025.112750
    2. Stephanie X. Wang, J. Herbert Waite. Catechol redox maintenance in mussel adhesion. Nature Reviews Chemistry, 2025, 9(3): 159. doi:10.1038/s41570-024-00673-4
    3. 昊勋 张, 明松 李, 永云 胡. 古气候数据同化: 原理和展望. SCIENTIA SINICA Terrae, 2025. doi:10.1360/SSTe-2024-0090
    4. Hana Jurikova, Claudio Garbelli, Ross Whiteford, et al. Rapid rise in atmospheric CO2 marked the end of the Late Palaeozoic Ice Age. Nature Geoscience, 2025, 18(1): 91. doi:10.1038/s41561-024-01610-2
    5. Md Anwar Nawaz, Mehraj ud din War, Gurunathan Baskar, et al. Unveiling the ecology of planktonic harpacticoids (Harpacticoida: Copepoda) in a stressed tropical coastal ecosystem, Bay of Bengal, India. Aquatic Ecology, 2025, 59(1): 159. doi:10.1007/s10452-024-10154-x
    6. Haoxun Zhang, Mingsong Li, Yongyun Hu. Paleoclimate data assimilation: Principles and prospects. Science China Earth Sciences, 2025, 68(2): 407. doi:10.1007/s11430-024-1439-y
    7. Congcong Wang, Yewei Yu, Facundo Llompart, et al. Environmental DNA as a novel tool for monitoring fish community structure and diversity feature in the northern Antarctic Peninsula. Estuarine, Coastal and Shelf Science, 2025, 313: 109076. doi:10.1016/j.ecss.2024.109076
    8. Manuel Andreas Staggl, Carlos De Gracia, Faviel A. López-Romero, et al. The Drivers of Mesozoic Neoselachian Success and Resilience. Biology, 2025, 14(2): 142. doi:10.3390/biology14020142
    9. Zhi-Guo Dong, Bang-Lu Zhang, Lian-Chang Zhang, et al. Unravelling the mechanisms underlying marine redox shifts during sedimentary manganese metallogenesis: insights from the Carboniferous Muhu deposit, China. Mineralium Deposita, 2025. doi:10.1007/s00126-024-01343-7
    10. Christopher R. Scotese, Christian Vérard, Landon Burgener, et al. The Cretaceous world: plate tectonics, palaeogeography and palaeoclimate. Geological Society, London, Special Publications, 2025, 544(1): 31. doi:10.1144/SP544-2024-28
    11. Ninon Allaire, Dieter Korn, Diego Balseiro, et al. Biodiversity dynamics during the initial Devonian radiation of ammonoids. Earth-Science Reviews, 2025, 264: 105090. doi:10.1016/j.earscirev.2025.105090
    12. Haowei Cai, Mo Zhang, Rui Gao, et al. Effects of intermittent fasting on behavioral and physiological stress indicators in Pacific abalone during persistent ocean heat waves. Aquaculture, 2025, 602: 742367. doi:10.1016/j.aquaculture.2025.742367
    13. Xin Sun, Li Tian, Xincheng Qiu, et al. Gastropod Fauna of the Zuodeng Permian-Triassic Boundary Section in the Nanpanjiang Basin and Its Geometric-Based Morphological Disparity Analysis. Journal of Earth Science, 2025, 36(1): 89. doi:10.1007/s12583-022-1645-x
    14. Weihong He, G.R. Shi, Kexin Zhang, et al. The deterioration and collapse of late Permian marine ecosystems and the end-Permian mass extinction: A global view. Earth-Science Reviews, 2025, 261: 104971. doi:10.1016/j.earscirev.2024.104971
    15. Kun Liang, Mikołaj K. Zapalski, Le Yao, et al. Editorial preface to special issue: Paleoecology and evolution of Paleozoic corals and reef ecosystems. Palaeogeography, Palaeoclimatology, Palaeoecology, 2024, 655: 112471. doi:10.1016/j.palaeo.2024.112471
    16. Kangyue Wu, Bin Xiu, Dandan Cui, et al. Composition and distribution of nutrients and environmental capacity in Dapeng Bay, northern South China Sea. Marine Pollution Bulletin, 2024, 206: 116689. doi:10.1016/j.marpolbul.2024.116689
    17. Riccardo Gerin, Riccardo Martellucci, Gilda Savonitto, et al. Correction and harmonization of dissolved oxygen data from autonomous platforms in the South Adriatic Pit (Mediterranean Sea). Frontiers in Marine Science, 2024, 11 doi:10.3389/fmars.2024.1373196
    18. Sajad A. Abdullah, Kadhim F. Kadhim, Yasser W. Ouda, et al. Ecological dynamics of Al-Chibayish marshes in southern Iraq: Insights into water quality, fish genetic affinity, and conservation implications. Heliyon, 2024, 10(14): e34332. doi:10.1016/j.heliyon.2024.e34332
    19. Alexander Ruebenstahl, Nicolás Mongiardino Koch, James C. Lamsdell, et al. Convergent evolution of giant size in eurypterids. Proceedings of the Royal Society B: Biological Sciences, 2024, 291(2027) doi:10.1098/rspb.2024.1184
    20. Fengjiao Liu, Lingling Su, Yanting Du, et al. No-interfered and visual evaluation of global warming impacts on phytoplankton-based copper bioavailability and then carbon sequestration. Science of The Total Environment, 2024, 948: 174762. doi:10.1016/j.scitotenv.2024.174762
    21. Bo Ping, Yunshan Meng, Fenzhen Su, et al. Retrieval of subsurface dissolved oxygen from surface oceanic parameters based on machine learning. Marine Environmental Research, 2024, 199: 106578. doi:10.1016/j.marenvres.2024.106578
    22. Zhongzhao Ding, Zhixin Ma, Shixue Hu, et al. Paleoclimate evolution of the Middle Triassic Guanling Formation from South China and its significance for the preservation of the Luoping biota. Global and Planetary Change, 2024, 242: 104588. doi:10.1016/j.gloplacha.2024.104588
    23. Hyeonho An, Jaewoo Jung, Huijeong Hwang, et al. Uncovering the oxic-suboxic microenvironment change in seamount flank through authigenic clay minerals in basaltic substrate of ferromanganese crust, Magellan seamount. Frontiers in Marine Science, 2024, 11 doi:10.3389/fmars.2024.1481396
    24. Demetris Koutsoyiannis. Stochastic assessment of temperature–CO2 causal relationship in climate from the Phanerozoic through modern times. Mathematical Biosciences and Engineering, 2024, 21(7): 6560. doi:10.3934/mbe.2024287
    25. Haitao Shang. Scale-Independent Variation Rates of Phanerozoic Environmental Variables and Implications for Earth’s Sustainability and Habitability. Mathematical Geosciences, 2024, 56(7): 1469. doi:10.1007/s11004-024-10135-8
    26. Kang Liu, Maosheng Jiang, Pan Tang, et al. Persistent cooling in the Ordovician (Darriwilian–Sandbian) revealed by conodont δ18O records in the Tarim Basin, NW China: Climatic and sedimentary implications. Palaeogeography, Palaeoclimatology, Palaeoecology, 2024, 650: 112371. doi:10.1016/j.palaeo.2024.112371
    27. Sophie Westacott, Mingyu Zhao, Lidya G. Tarhan. Extent and biogeochemical impact of Skolithos piperock in the lower Cambrian Zabriskie Quartzite (California, USA). Palaeogeography, Palaeoclimatology, Palaeoecology, 2024, 651: 112381. doi:10.1016/j.palaeo.2024.112381
    28. Shaun Lovejoy, Andrej Spiridonov. The Fractional MacroEvolution Model: a simple quantitative scaling macroevolution model. Paleobiology, 2024, 50(2): 376. doi:10.1017/pab.2023.38
    29. Kilian Eichenseer, Lewis A. Jones. Bayesian multi-proxy reconstruction of early Eocene latitudinal temperature gradients. Climate of the Past, 2024, 20(2): 349. doi:10.5194/cp-20-349-2024
    30. Shaghayegh Sadat Hashempour, Sajjad Maghfouri, Ebrahim Rastad, et al. Metallogeny and temporal-spatial distribution of sedimentary phosphorite mineralization in Iran, relation to tethyans oceans evaluation and implications for future exploration. Ore Geology Reviews, 2024, 164: 105855. doi:10.1016/j.oregeorev.2023.105855
    31. K. Vasileva, M. Rogov, V. Ershova, et al. Ikaite versus seep-related carbonate precipitation in the Late Jurassic–Early Cretaceous of West Spitsbergen: evidence for cold versus warm climates?. International Journal of Earth Sciences, 2024, 113(2): 417. doi:10.1007/s00531-023-02380-9
    32. Zhenguo Wang, Cunjin Xue, Bo Ping. A Reconstructing Model Based on Time–Space–Depth Partitioning for Global Ocean Dissolved Oxygen Concentration. Remote Sensing, 2024, 16(2): 228. doi:10.3390/rs16020228
    33. Emily J. Judd, Jessica E. Tierney, Daniel J. Lunt, et al. A 485-million-year history of Earth’s surface temperature. Science, 2024, 385(6715) doi:10.1126/science.adk3705
    34. Chang Lu, Xin-Dong Cui, Jun Chen, et al. Devonian sea surface temperature and paleoecology changes constrained by in situ oxygen isotopes of fish fossils. Palaeogeography, Palaeoclimatology, Palaeoecology, 2024, 639: 112059. doi:10.1016/j.palaeo.2024.112059
    35. Alice M. Clement, Richard Cloutier, Michael S. Y. Lee, et al. A Late Devonian coelacanth reconfigures actinistian phylogeny, disparity, and evolutionary dynamics. Nature Communications, 2024, 15(1) doi:10.1038/s41467-024-51238-4
    36. Joseph T. Flannery-Sutherland, Cameron D. Crossan, Corinne E. Myers, et al. Late Cretaceous ammonoids show that drivers of diversification are regionally heterogeneous. Nature Communications, 2024, 15(1) doi:10.1038/s41467-024-49462-z
    37. Ines Haberle, Domagoj K. Hackenberger, Tamara Djerdj, et al. Effects of climate change on gilthead seabream aquaculture in the Mediterranean. Aquaculture, 2024, 578: 740052. doi:10.1016/j.aquaculture.2023.740052
    38. Trond H. Torsvik, Dana L. Royer, Chloe M. Marcilly, et al. User-friendly carbon-cycle modelling and aspects of Phanerozoic climate change. Applied Computing and Geosciences, 2024, 23: 100180. doi:10.1016/j.acags.2024.100180
    39. A.M. Mancini, F. Lozar, R. Gennari, et al. The past to unravel the future: Deoxygenation events in the geological archive and the anthropocene oxygen crisis. Earth-Science Reviews, 2024, 249: 104664. doi:10.1016/j.earscirev.2023.104664
    40. B. Křížová, L. Consorti, S. Cardelli, et al. Late Cretaceous (Cenomanian-Turonian) temperature evolution and biotic response in the Adriatic Carbonate Platform region of Friuli, northeast Italy. Palaeogeography, Palaeoclimatology, Palaeoecology, 2024, 637: 111995. doi:10.1016/j.palaeo.2023.111995
    41. Md. Anwar Nawaz, Kandhasamy Sivakumar, Gurunathan Baskar. Seasonal dynamics of body size in calanoid copepods (Calanoida: Copepoda) from the stressed tropical coast of India, Chennai, Bay of Bengal. Aquatic Ecology, 2024, 58(2): 363. doi:10.1007/s10452-023-10075-1
    42. Haitao Shang. Dichotomous effects of oxidative metabolisms: A theoretical perspective on the dolomite problem. Global and Planetary Change, 2023, 222: 104041. doi:10.1016/j.gloplacha.2023.104041
    43. 力 田, 海军 宋, 羽初 刘, et al. 显生宙古海洋环境和气候波动与特提斯演化. SCIENTIA SINICA Terrae, 2023, 53(12): 2830. doi:10.1360/SSTe-2023-0041
    44. Bo Chen, Maoyan Zhu. Oxygen isotope application in paleotemperature reconstruction and water cycle in the deep time. Chinese Science Bulletin, 2023, 68(12): 1528. doi:10.1360/TB-2022-1181
    45. Alexandre Pohl, Richard G. Stockey, Xu Dai, et al. Why the Early Paleozoic was intrinsically prone to marine extinction. Science Advances, 2023, 9(35) doi:10.1126/sciadv.adg7679
    46. Yanming Zhang, Hongtao Nie, Xiwu Yan. Transient receptor potential (TRP) channels in the Manila clam (Ruditapes philippinarum): Characterization and expression patterns of the TRP gene family under heat stress in Manila clams based on genome-wide identification. Gene, 2023, 854: 147112. doi:10.1016/j.gene.2022.147112
    47. Landon Burgener, Ethan Hyland, Brian J. Reich, et al. Cretaceous climates: Mapping paleo-Köppen climatic zones using a Bayesian statistical analysis of lithologic, paleontologic, and geochemical proxies. Palaeogeography, Palaeoclimatology, Palaeoecology, 2023, 613: 111373. doi:10.1016/j.palaeo.2022.111373
    48. Lilian B. Pérez-Sosa, Miguel Nakamura, Pablo Del Monte-Luna, et al. Role of Taxa Age and Geologic Range: Survival Analysis of Marine Biota over the Last 538 Million Years. Journal of Agricultural, Biological and Environmental Statistics, 2023, 28(4): 684. doi:10.1007/s13253-023-00547-0
    49. Seth A. Young, Cole T. Edwards, Leho Ainsaar, et al. Seawater signatures of Ordovician climate and environment. Geological Society, London, Special Publications, 2023, 532(1): 137. doi:10.1144/SP532-2022-258
    50. Li Tian, Haijun Song, Yuchu Liu, et al. Phanerozoic oceanic and climatic perturbations in the context of Tethyan evolution. Science China Earth Sciences, 2023, 66(12): 2791. doi:10.1007/s11430-023-1205-6
    51. Daniel Eliahou Ontiveros, Gregory Beaugrand, Bertrand Lefebvre, et al. Impact of global climate cooling on Ordovician marine biodiversity. Nature Communications, 2023, 14(1) doi:10.1038/s41467-023-41685-w
    52. Penpicha Satanwat, Paveena Tapaneeyaworawong, Piyanuch Wechprasit, et al. Total ammonia nitrogen removal and microbial community dynamics in an outdoor HDPE-lined shrimp pond with no water discharge. Aquaculture, 2023, 577: 739898. doi:10.1016/j.aquaculture.2023.739898
    53. Md Anwar Nawaz, Sivakumar Kandhasamy, Baskar Gurunathan. Impact of Variation in Environmental Parameters on Abundance of Paracalanidae (Calanoida: Copepoda) from the Tropical Coast of India, Bay of Bengal. Russian Journal of Marine Biology, 2023, 49(5): 391. doi:10.1134/S1063074023050073
    54. Daniela S. Monti, Viviana A. Confalonieri, M. Franco Tortello. The Central Andean Basin as a dispersal centre: Biogeographic patterns of olenid trilobites during the late Cambrian – Early Ordovician. Palaeogeography, Palaeoclimatology, Palaeoecology, 2023, 618: 111519. doi:10.1016/j.palaeo.2023.111519
    55. Andrea Baucon, Annalisa Ferretti, Chiara Fioroni, et al. The earliest evidence of deep-sea vertebrates. Proceedings of the National Academy of Sciences, 2023, 120(37) doi:10.1073/pnas.2306164120
    56. Liuhuo Wang, Qingcui Liu, Wenwei Zhu, et al. Research on Electromagnetic Loss Characteristics of Submarine Cables. Energy Engineering, 2023, 120(11): 2651. doi:10.32604/ee.2023.027791
    57. Le Yao, Stephen Kershaw, Shuzhong Shen, et al. A new reef classification model with insights into Phanerozoic evolution of reef ecosystems. Sedimentology, 2023, 70(6): 1886. doi:10.1111/sed.13099
    58. Maoyan Zhu, Zhengtang Guo, Pinxian Wang. Evolution of water cycle in deep time: Current research status and key questions. Chinese Science Bulletin, 2023, 68(12): 1425. doi:10.1360/TB-2022-1285
    59. Nussaïbah B. Raja, John M. Pandolfi, Wolfgang Kiessling. Modularity explains large-scale reef booms in Earth’s history. Facies, 2023, 69(3) doi:10.1007/s10347-023-00671-w
    60. Minghong Peng, Jingchun Tian, Xiang Zhang, et al. Controls on organic matter accumulation on the Late-Ordovician shales in Awati Sag in northwestern Tarim Basin, NW China. Geoenergy Science and Engineering, 2023, 221: 111308. doi:10.1016/j.petrol.2022.111308
    61. Chuanzhen Ren, Qiang Fang, Huaichun Wu, et al. Cyclostratigraphic correlation of Middle–Late Ordovician sedimentary successions between the South China Block and Tarim Basin with paleoclimatic and geochronological implications. Journal of Asian Earth Sciences, 2023, 246: 105577. doi:10.1016/j.jseaes.2023.105577
    62. Mohamed Tawfik, Abelbaset S. El-Sorogy, Khaled Al-Kahtany. Facies Associations and Sequence Stratigraphy of the Toarcian Marrat Formation (Saudi Arabia) and Their Equivalents in Some Gondwanaland Regions. Journal of Earth Science, 2023, 34(1): 242. doi:10.1007/s12583-020-1379-6
    63. David R. Cordie. Analysis of the environmental impacts affecting Cambrian reef building and carbonate settings during the Miaolingian and Furongian epochs: A hypothesis for consideration. Evolving Earth, 2023, 1: 100002. doi:10.1016/j.eve.2023.100002
    64. Xueqian Fu, Haosen Niu. Key technologies and applications of agricultural energy Internet for agricultural planting and fisheries industry. Information Processing in Agriculture, 2023, 10(3): 416. doi:10.1016/j.inpa.2022.10.004
    65. Nir J. Shaviv, Henrik Svensmark, Ján Veizer. The Phanerozoic climate. Annals of the New York Academy of Sciences, 2023, 1519(1): 7. doi:10.1111/nyas.14920
    66. Marwa I. Farghaly, Tamer El-Sayed Ali, Hanan M. Mitwally, et al. Reproductive studies on the carpet clam Paphia textile (Paratapes textilis) (Gmelin 1791) (Family: Veneridae): a guide of aquaculture management along the Egyptian coasts of the Red Sea and Suez Canal. BMC Zoology, 2023, 8(1) doi:10.1186/s40850-023-00179-4
    67. J. Fred Read, Michael C. Pope, Maya Elrick, et al. Depositional and tectonic influences on preservation of Milankovitch record during long-term global cooling: Middle and Upper Ordovician convergent foreland, eastern USA. Palaeogeography, Palaeoclimatology, Palaeoecology, 2023, 627: 111738. doi:10.1016/j.palaeo.2023.111738
    68. Yanming Zhang, Hongtao Nie, Xiwu Yan. Metabolomic analysis provides new insights into the heat-hardening response of Manila clam (Ruditapes philippinarum) to high temperature stress. Science of The Total Environment, 2023, 857: 159430. doi:10.1016/j.scitotenv.2022.159430
    69. Zihu Zhang, Meng Cheng, Haiyang Wang, et al. Spatiotemporal variation of dissolved oxygen in the Ediacaran surface ocean and its implication for oceanic carbon cycling. Science China Earth Sciences, 2023, 66(8): 1892. doi:10.1007/s11430-022-1116-3
    70. Anders Lindskog, Seth A. Young, Chelsie N. Bowman, et al. Oxygenation of the Baltoscandian shelf linked to Ordovician biodiversification. Nature Geoscience, 2023, 16(11): 1047. doi:10.1038/s41561-023-01287-z
    71. Di Chen, Bing Huang, Yves Candela. Evolutionary trends in trimerellid brachiopods. Palaeogeography, Palaeoclimatology, Palaeoecology, 2023, 617: 111472. doi:10.1016/j.palaeo.2023.111472
    72. Chloé M. Marcilly, Pierre Maffre, Guillaume Le Hir, et al. Understanding the early Paleozoic carbon cycle balance and climate change from modelling. Earth and Planetary Science Letters, 2022, 594: 117717. doi:10.1016/j.epsl.2022.117717
    73. Valentin Bault, Diego Balseiro, Claude Monnet, et al. Post-Ordovician trilobite diversity and evolutionary faunas. Earth-Science Reviews, 2022, 230: 104035. doi:10.1016/j.earscirev.2022.104035
    74. Tarini Prasad Sahoo, Sonpal Vasavdutta, Amit Chanchpara, et al. Pre-to-post COVID-19 lockdown and their environmental impacts on Ghoghla beach and Somnath beach, India. Environmental Science and Pollution Research, 2022, 29(54): 82140. doi:10.1007/s11356-022-21586-z
    75. Zhengquan Zhou, Tjeerd J. Bouma, Gregory S. Fivash, et al. Thermal stress affects bioturbators' burrowing behavior: A mesocosm experiment on common cockles (Cerastoderma edule). Science of The Total Environment, 2022, 824: 153621. doi:10.1016/j.scitotenv.2022.153621
    76. Ardiansyah Koeshidayatullah, Elizabeth J. Trower, Xiaowei Li, et al. Quantitative evaluation of the roles of ocean chemistry and climate on ooid size across the Phanerozoic: Global versus local controls. Sedimentology, 2022, 69(6): 2486. doi:10.1111/sed.12998
    77. Andrej Spiridonov, Shaun Lovejoy. Life rather than climate influences diversity at scales greater than 40 million years. Nature, 2022, 607(7918): 307. doi:10.1038/s41586-022-04867-y
    78. Hongrui Zhang, Trond H. Torsvik. Circum-Tethyan magmatic provinces, shifting continents and Permian climate change. Earth and Planetary Science Letters, 2022, 584: 117453. doi:10.1016/j.epsl.2022.117453
    79. Kang Liu, Maosheng Jiang, Liyu Zhang, et al. A new high-resolution palaeotemperature record during the Middle–Late Ordovician transition derived from conodont δ 18 O palaeothermometry. Journal of the Geological Society, 2022, 179(4) doi:10.1144/jgs2021-148
    80. Ethan L. Grossman, Michael M. Joachimski. Ocean temperatures through the Phanerozoic reassessed. Scientific Reports, 2022, 12(1) doi:10.1038/s41598-022-11493-1
    81. Kang Liu, Maosheng Jiang, Taiyu Huang, et al. A reassessment on the timing and potential drivers of the major seawater 87Sr/86Sr drop in the Ordovician Period: New evidence from conodonts in China. Chemical Geology, 2022, 604: 120906. doi:10.1016/j.chemgeo.2022.120906
    82. Lewis A. Jones, Kilian Eichenseer. Uneven spatial sampling distorts reconstructions of Phanerozoic seawater temperature. Geology, 2022, 50(2): 238. doi:10.1130/G49132.1
    83. Junpeng Zhang, Chao Li, Yuandong Zhang. Geological evidences and mechanisms for oceanic anoxic events during the Early Paleozoic. Chinese Science Bulletin, 2022, 67(15): 1644. doi:10.1360/TB-2021-0535
    84. C N P Wibowo, L Sulmartiwi, S Andriyono. Correlation Between Water Quality to Blood Glucose of Cantang Grouper (E. fuscoguttatus x E. lanceolatus) as an Indicator of Stress in Floating Net Cage. IOP Conference Series: Earth and Environmental Science, 2022, 1036(1): 012084. doi:10.1088/1755-1315/1036/1/012084
    85. Junxian Wang, Pingchang Sun, Yueyue Bai, et al. Carbon isotopes of n-alkanes allow for estimation of the CO2 pressure in the Early Jurassic - A case study from lacustrine shale and cannel boghead in the Dachanggou Basin, Xinjiang, Northwest China. Palaeogeography, Palaeoclimatology, Palaeoecology, 2022, 607: 111252. doi:10.1016/j.palaeo.2022.111252
    86. Dmitry A. Ruban. A review of the Late Triassic conodont conundrum: survival beyond biotic perturbations. Palaeobiodiversity and Palaeoenvironments, 2022, 102(2): 373. doi:10.1007/s12549-021-00505-z
    87. Zhongshi Zhang, Shuanglin Li, Huijun Wang, et al. 浅谈大气科学与地质学的学科交叉. Earth Science-Journal of China University of Geosciences, 2022, 47(10): 3569. doi:10.3799/dqkx.2022.350
    88. Suman Halder, Susanne K. M. Arens, Kai Jensen, et al. A dynamic local-scale vegetation model for lycopsids (LYCOm v1.0). Geoscientific Model Development, 2022, 15(5): 2325. doi:10.5194/gmd-15-2325-2022
    89. Douwe G. van der Meer, Christopher R. Scotese, Benjamin J.W. Mills, et al. Long-term Phanerozoic global mean sea level: Insights from strontium isotope variations and estimates of continental glaciation. Gondwana Research, 2022, 111: 103. doi:10.1016/j.gr.2022.07.014
    90. Siyumini Perera, Jonathan C. Aitchison. Late Sandbian (Sa2) radiolarians of the Pingliang Formation from the Guanzhuang section, Gansu Province, China. Journal of Paleontology, 2022, 96(1): 19. doi:10.1017/jpa.2021.86
    91. Xiuchun Jing, Zhenyu Zhao, Ling Fu, et al. Biostratigraphically-controlled Darriwilian (Middle Ordovician) δ13C excursions in North China: Implications for correlation and climate change. Palaeogeography, Palaeoclimatology, Palaeoecology, 2022, 601: 111149. doi:10.1016/j.palaeo.2022.111149
    92. Haozhe Wang, Qian Deng, Bin Cheng, et al. Synchronous positive δ13Ccarb and δ13Corg excursions during 497–494 Ma: From a CO2 concentrating mechanism dominated photosynthesis?. Palaeogeography, Palaeoclimatology, Palaeoecology, 2022, 602: 111160. doi:10.1016/j.palaeo.2022.111160
    93. Farideh Moharrek, Paul D. Taylor, Daniele Silvestro, et al. Diversification dynamics of cheilostome bryozoans based on a Bayesian analysis of the fossil record. Palaeontology, 2022, 65(1) doi:10.1111/pala.12586
    94. Emily J. Judd, Jessica E. Tierney, Brian T. Huber, et al. The PhanSST global database of Phanerozoic sea surface temperature proxy data. Scientific Data, 2022, 9(1) doi:10.1038/s41597-022-01826-0
    95. Paul J. Valdes, Christopher R. Scotese, Daniel J. Lunt. Deep ocean temperatures through time. Climate of the Past, 2021, 17(4): 1483. doi:10.5194/cp-17-1483-2021
    96. Dongyang Liu, Chunju Huang, James G. Ogg, et al. Astronomically forced changes in chemical weathering and redox during the Anisian (Middle Triassic): Implications for marine ecosystem recovery following the end-Permian mass extinction. Palaeogeography, Palaeoclimatology, Palaeoecology, 2021, 569: 110355. doi:10.1016/j.palaeo.2021.110355
    97. Shahab Varkouhi, Luis Miguel Jaques Ribeiro. Bimineralic Middle Triassic ooids from Hydra Island: Diagenetic pathways and implications for ancient seawater geochemistry. The Depositional Record, 2021, 7(2): 344. doi:10.1002/dep2.117
    98. Bolin Zhang, Paul B. Wignall, Suping Yao, et al. Collapsed upwelling and intensified euxinia in response to climate warming during the Capitanian (Middle Permian) mass extinction. Gondwana Research, 2021, 89: 31. doi:10.1016/j.gr.2020.09.003
    99. L. Robin M. Cocks, Trond H. Torsvik. Ordovician palaeogeography and climate change. Gondwana Research, 2021, 100: 53. doi:10.1016/j.gr.2020.09.008
    100. Yanyang Pan, Xinghua Lin, Fangyuan Chen, et al. Genome-wide identification and expression profiling of glutathione S-transferase family under hypoxia stress in silver sillago (Sillago sihama). Comparative Biochemistry and Physiology Part D: Genomics and Proteomics, 2021, 40: 100920. doi:10.1016/j.cbd.2021.100920
    101. Marie Laugié, Yannick Donnadieu, Jean‐Baptiste Ladant, et al. Exploring the Impact of Cenomanian Paleogeography and Marine Gateways on Oceanic Oxygen. Paleoceanography and Paleoclimatology, 2021, 36(7) doi:10.1029/2020PA004202
    102. Yilun Yu, Chi Zhang, Xing Xu. Deep time diversity and the early radiations of birds. Proceedings of the National Academy of Sciences, 2021, 118(10) doi:10.1073/pnas.2019865118
    103. Junpeng Zhang, Cole T. Edwards, Charles W. Diamond, et al. Marine oxygenation, deoxygenation, and life during the Early Paleozoic: An overview. Palaeogeography, Palaeoclimatology, Palaeoecology, 2021, 584: 110715. doi:10.1016/j.palaeo.2021.110715
    104. Chloé M. Marcilly, Trond H. Torsvik, Mathew Domeier, et al. New paleogeographic and degassing parameters for long-term carbon cycle models. Gondwana Research, 2021, 97: 176. doi:10.1016/j.gr.2021.05.016
    105. Gregor H. Mathes, Jeroen van Dijk, Wolfgang Kiessling, et al. Extinction risk controlled by interaction of long-term and short-term climate change. Nature Ecology & Evolution, 2021, 5(3): 304. doi:10.1038/s41559-020-01377-w
    106. Xiaocong Luan, Xiaole Zhang, Rongchang Wu, et al. Environmental changes revealed by Lower–Middle Ordovician deeper-water marine red beds from the marginal Yangtze Platform, South China: Links to biodiversification. Palaeogeography, Palaeoclimatology, Palaeoecology, 2021, 562: 110116. doi:10.1016/j.palaeo.2020.110116
    107. Zhongyang Chen, Peep Männik, Junxuan Fan, et al. Age of the Silurian Lower Red Beds in South China: Stratigraphical Evidence from the Sanbaiti Section. Journal of Earth Science, 2021, 32(3): 524. doi:10.1007/s12583-020-1350-6
    108. Nicola Conci, Sergio Vargas, Gert Wörheide. The Biology and Evolution of Calcite and Aragonite Mineralization in Octocorallia. Frontiers in Ecology and Evolution, 2021, 9 doi:10.3389/fevo.2021.623774
    109. Luca Medici, Martina Savioli, Annalisa Ferretti, et al. Zooming in REE and Other Trace Elements on Conodonts: Does Taxonomy Guide Diagenesis?. Journal of Earth Science, 2021, 32(3): 501. doi:10.1007/s12583-020-1094-3
    110. Haijun Song, David B. Kemp, Li Tian, et al. Thresholds of temperature change for mass extinctions. Nature Communications, 2021, 12(1) doi:10.1038/s41467-021-25019-2
    111. Yixin Dong, Ying Cui, Jiuyuan Wang, et al. Paleozoic carbon cycle dynamics: Insights from stable carbon isotopes in marine carbonates and C3 land plants. Earth-Science Reviews, 2021, 222: 103813. doi:10.1016/j.earscirev.2021.103813
    112. Alexandra J. Buczek, Austin J.W. Hendy, Melanie J. Hopkins, et al. On the reconciliation of biostratigraphy and strontium isotope stratigraphy of three southern Californian Plio-Pleistocene formations. GSA Bulletin, 2021, 133(1-2): 100. doi:10.1130/B35488.1
    113. Yan Feng, Haijun Song, David P. G. Bond. Size variations in foraminifers from the early Permian to the Late Triassic: implications for the Guadalupian–Lopingian and the Permian–Triassic mass extinctions. Paleobiology, 2020, 46(4): 511. doi:10.1017/pab.2020.37
    114. Zhang Xinsong, Li Siyu, Song Yinfan, et al. Size reduction of conodonts indicates high ecological stress during the late Frasnian under greenhouse climate conditions in South China. Palaeogeography, Palaeoclimatology, Palaeoecology, 2020, 556: 109909. doi:10.1016/j.palaeo.2020.109909
    115. Shouyi Jiang, Haijun Song, David B. Kemp, et al. Two pulses of extinction of larger benthic foraminifera during the Pliensbachian-Toarcian and early Toarcian environmental crises. Palaeogeography, Palaeoclimatology, Palaeoecology, 2020, 560: 109998. doi:10.1016/j.palaeo.2020.109998
    116. Samuel Ginot, Nicolas Goudemand. Global climate changes account for the main trends of conodont diversity but not for their final demise. Global and Planetary Change, 2020, 195: 103325. doi:10.1016/j.gloplacha.2020.103325
    117. Lihao Wang, Yu Jiang, Hong Qi. Marine Dissolved Oxygen Prediction With Tree Tuned Deep Neural Network. IEEE Access, 2020, 8: 182431. doi:10.1109/ACCESS.2020.3028863
    118. Decan Tan, Jian-Ming Zhu, Xiangli Wang, et al. Equilibrium fractionation and isotope exchange kinetics between aqueous Se(IV) and Se(VI). Geochimica et Cosmochimica Acta, 2020, 277: 21. doi:10.1016/j.gca.2020.03.017
    119. Noah T. Anderson, Clinton A. Cowan, Kristin D. Bergmann. A case for the growth of ancient ooids within the sediment pile. Journal of Sedimentary Research, 2020, 90(8): 843. doi:10.2110/jsr.2020.45
    120. David P.G. Bond, Paul B. Wignall, Stephen E. Grasby. The Capitanian (Guadalupian, Middle Permian) mass extinction in NW Pangea (Borup Fiord, Arctic Canada): A global crisis driven by volcanism and anoxia. GSA Bulletin, 2020, 132(5-6): 931. doi:10.1130/B35281.1
    121. Roquia Rizk, Tatjána Juzsakova, Igor Cretescu, et al. Environmental assessment of physical-chemical features of Lake Nasser, Egypt. Environmental Science and Pollution Research, 2020, 27(16): 20136. doi:10.1007/s11356-020-08366-3
    122. Haijun Song, Shan Huang, Enhao Jia, et al. Flat latitudinal diversity gradient caused by the Permian–Triassic mass extinction. Proceedings of the National Academy of Sciences, 2020, 117(30): 17578. doi:10.1073/pnas.1918953117
    123. Mingtao Li, Haijun Song, Adam D. Woods, et al. Facies and evolution of the carbonate factory during the Permian–Triassic crisis in South Tibet, China. Sedimentology, 2019, 66(7): 3008. doi:10.1111/sed.12619
    124. Christian Vérard, Ján Veizer. On plate tectonics and ocean temperatures. Geology, 2019, 47(9): 881. doi:10.1130/G46376.1
    125. Mu Liu, Daizhao Chen, Xiqiang Zhou, et al. Upper Ordovician marine red limestones, Tarim Basin, NW China: A product of an oxygenated deep ocean and changing climate?. Global and Planetary Change, 2019, 183: 103032. doi:10.1016/j.gloplacha.2019.103032
    126. Jorge García Molinos, Irene D. Alabia. Biogeography. doi:10.1002/9781119882381.ch10
    127. Angela Lis, Viorica Gladchi, Gheorghe Duca, et al. Environmental and Technological Aspects of Redox Processes. Advances in Environmental Engineering and Green Technologies, doi:10.4018/979-8-3693-0512-6.ch003
    128. Wei-Hong He, G. R. Shi, Ke-Xin Zhang, et al. Stratigraphy Around the Permian–Triassic Boundary of South China. New Records of the Great Dying in South China, doi:10.1007/978-981-99-9350-5_5
    129. Jianing Yang. Proceedings of the 6th International Conference on Economic Management and Green Development. Applied Economics and Policy Studies, doi:10.1007/978-981-19-7826-5_14
    130. Viorica Gladchi, Elena Bunduchi, Gheorghe Duca, et al. Environmental and Technological Aspects of Redox Processes. Advances in Environmental Engineering and Green Technologies, doi:10.4018/979-8-3693-0512-6.ch002

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    Created with Highcharts 5.0.7Chart context menuAccess Area Distribution其他: 2.4 %其他: 2.4 %Algeria: 0.1 %Algeria: 0.1 %Argentina: 0.2 %Argentina: 0.2 %Australia: 1.0 %Australia: 1.0 %Austria: 0.1 %Austria: 0.1 %Belgium: 0.3 %Belgium: 0.3 %Brazil: 0.3 %Brazil: 0.3 %Brunei Darussalam: 0.1 %Brunei Darussalam: 0.1 %Bulgaria: 0.2 %Bulgaria: 0.2 %Cameroon: 0.1 %Cameroon: 0.1 %Canada: 0.7 %Canada: 0.7 %Chile: 0.4 %Chile: 0.4 %China: 20.8 %China: 20.8 %Croatia (LOCAL Name: Hrvatska): 0.2 %Croatia (LOCAL Name: Hrvatska): 0.2 %Czech Republic: 0.2 %Czech Republic: 0.2 %Denmark: 0.3 %Denmark: 0.3 %Dominican Republic: 0.1 %Dominican Republic: 0.1 %Egypt: 0.3 %Egypt: 0.3 %Estonia: 0.1 %Estonia: 0.1 %Finland: 0.2 %Finland: 0.2 %France: 1.2 %France: 1.2 %Germany: 1.2 %Germany: 1.2 %Gibraltar: 0.2 %Gibraltar: 0.2 %Greece: 0.6 %Greece: 0.6 %Hong Kong, China: 0.7 %Hong Kong, China: 0.7 %Hungary: 0.1 %Hungary: 0.1 %Iceland: 0.1 %Iceland: 0.1 %India: 1.0 %India: 1.0 %Indonesia: 0.6 %Indonesia: 0.6 %Iran (ISLAMIC Republic Of): 0.1 %Iran (ISLAMIC Republic Of): 0.1 %Ireland: 0.2 %Ireland: 0.2 %Italy: 0.6 %Italy: 0.6 %Japan: 1.2 %Japan: 1.2 %Kenya: 0.1 %Kenya: 0.1 %Korea Republic of: 1.6 %Korea Republic of: 1.6 %Malaysia: 0.3 %Malaysia: 0.3 %Mexico: 0.3 %Mexico: 0.3 %Morocco: 0.1 %Morocco: 0.1 %Mozambique: 0.1 %Mozambique: 0.1 %Netherlands: 0.5 %Netherlands: 0.5 %New Zealand: 0.3 %New Zealand: 0.3 %Norway: 0.2 %Norway: 0.2 %Oman: 0.2 %Oman: 0.2 %Other: 0.2 %Other: 0.2 %Papua New Guinea: 0.1 %Papua New Guinea: 0.1 %Peru: 0.2 %Peru: 0.2 %Philippines: 0.6 %Philippines: 0.6 %Portugal: 0.1 %Portugal: 0.1 %Puerto Rico: 0.1 %Puerto Rico: 0.1 %Reserved: 6.2 %Reserved: 6.2 %Russian Federation: 6.3 %Russian Federation: 6.3 %Saudi Arabia: 0.1 %Saudi Arabia: 0.1 %Singapore: 1.1 %Singapore: 1.1 %South Africa: 0.1 %South Africa: 0.1 %Spain: 0.9 %Spain: 0.9 %Sweden: 0.1 %Sweden: 0.1 %Switzerland: 0.5 %Switzerland: 0.5 %Taiwan, China: 0.1 %Taiwan, China: 0.1 %Thailand: 0.1 %Thailand: 0.1 %Togo: 0.1 %Togo: 0.1 %Turkey: 0.6 %Turkey: 0.6 %United Arab Emirates: 0.5 %United Arab Emirates: 0.5 %United Kingdom: 1.7 %United Kingdom: 1.7 %United States: 39.9 %United States: 39.9 %Viet Nam: 0.3 %Viet Nam: 0.3 %罗奥尔凯埃: 0.1 %罗奥尔凯埃: 0.1 %其他AlgeriaArgentinaAustraliaAustriaBelgiumBrazilBrunei DarussalamBulgariaCameroonCanadaChileChinaCroatia (LOCAL Name: Hrvatska)Czech RepublicDenmarkDominican RepublicEgyptEstoniaFinlandFranceGermanyGibraltarGreeceHong Kong, ChinaHungaryIcelandIndiaIndonesiaIran (ISLAMIC Republic Of)IrelandItalyJapanKenyaKorea Republic ofMalaysiaMexicoMoroccoMozambiqueNetherlandsNew ZealandNorwayOmanOtherPapua New GuineaPeruPhilippinesPortugalPuerto RicoReservedRussian FederationSaudi ArabiaSingaporeSouth AfricaSpainSwedenSwitzerlandTaiwan, ChinaThailandTogoTurkeyUnited Arab EmiratesUnited KingdomUnited StatesViet Nam罗奥尔凯埃

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