RESEARCH ARTICLE
10.1029/2019JG005107
Key Points:• Extensive degradation of pre‐old OC
occurs in the Yangtze River estuary• Large OC 14C age heterogeneity isfound in northern Okinawa Troughsediment• Hydrodynamic processes exert astrong inﬂuence on 14C age
distribution of OM in continental
margin sediments
Supporting Information:• Supporting Information S1

Correspondence to:
R. Bao,Rui.Bao@aces.su.se

Citation:
Bao, R., Zhao, M., McNichol, A., Wu,
Y., Guo, X., Haghipour, N., & Eglinton,
T. I. (2019). On the origin of aged
sedimentary organic matter along ariver‐shelf‐deep ocean transect. Journalof Geophysical Research: Biogeosciences,
124, 2582–2594. https://doi.org/
10.1029/2019JG005107
Received 25 FEB 2019
Accepted 17 JUL 2019
Accepted article online 12 AUG 2019
Published online 29 AUG 2019

On the Origin of Aged Sedimentary Organic Matter Alonga River‐Shelf‐Deep Ocean Transect
Rui Bao1,2,3 , Meixun Zhao4,5, Ann McNichol2, Ying Wu6
Negar Haghipour1,8 , and Timothy I. Eglinton1, Xinyu Guo7,

1

Geological Institute, ETH Zurich, Zurich, Switzerland, 2National Ocean Science Accelerator Mass Spectrometry Facility,
Woods Hole Oceanographic Institute, Woods Hole, MA, USA, 3Department of Earth and Planetary Sciences, Harvard
University, Cambridge, MA, USA, 4Key Laboratory of Marine Chemistry Theory and Technology, Ministry of
Education/Institute for Advanced Ocean Studies, Ocean University of China, Qingdao, China, 5Laboratory for Marine
Ecology and Environmental Science, Qingdao National Laboratory for Marine Science and Technology, Qingdao, China,
6
State Key Laboratory of Estuarine and Coastal Research, East China Normal University, Shanghai, China, 7Center for
Marine Environmental Studies, Ehime University, Matsuyama, Japan, 8Laboratory for Ion Beam Physics, ETH Zurich,
Zurich, Switzerland

Abstract To assess the inﬂuences of carbon sources and transport processes on the 14C age oforganic matter (OM) in continental margin sediments, we examined a suite of samples collected along ariver‐shelf‐deep ocean transect in the East China Sea (ECS). Ramped pyrolysis‐oxidiation was conducted on
suspended particulate matter in the Yangtze River and on surface sediments from the ECS shelf andnorthern Okinawa Trough. 14C ages were determined on OM decomposition products within different
temperature windows. These measurements suggest that extensive amounts of pre‐old (i.e., millennial age)organic carbon (OC) are subject to degradation within and beyond the Yangtze River Delta, and this process
is accompanied by an exchange of terrestrial and marine OM. These results, combined with fatty acidconcentration data, suggest that both the nature and extent of OM preservation/degradation as well as themodes of transport inﬂuence the 14C ages of sedimentary OM. Additionally, we ﬁnd that the age of(thermally) refractory OC increases during across‐shelf transport and that the age offset between the lowest
and highest temperature OC decomposition fractions also increases along the shelf‐to‐trough transect.
Ampliﬁed interfraction spread or 14C heterogeneity is the greatest in the Okinawa Trough. Agedsedimentary OM across the transect may be a consequence of several reasons including fossil OC input,
selective degradation of younger OC, hydrodynamic sorting processes, and aging during lateral transport.
Consequently, each of them should be considered in assessing the 14C results of sedimentary OM and its
implications for the carbon cycle and interpretation of sedimentary records.

1. Introduction
Continental margins comprise the interface between land and deep ocean systems. Examination of changes
in content and composition of organic carbon (OC) along across‐margin transects on the interface representsa critical approach for understanding its role in the carbon cycle. Radiocarbon (14C) serves as a key property
for investigating OC cycle in this complex and dynamic regime. For river‐dominated margins, substantial
amounts of terrestrial organic matter (OM) are discharged to accumulate in coastal and shelf sediments(Bauer et al., 2013; Bianchi et al., 2017; Keil et al., 1997). This exported OM may derive from different terrestrial OC pools (e.g., fresh vascular plant debris, soil, and fossil OC eroded from sedimentary rocks) that vastlydiffer in 14C ages and residence times (Bao, Uchida, Zhao, et al., 2018; French et al., 2018; Galy et al., 2015; Wu
et al., 2018). In addition, continental shelf sediments also receive amounts of marine OC derived from primary productivity that is generally younger in 14C age by virtue of its recent synthesis and proximal source.
The OM accumulating in continental shelf surface sediments can exhibit spatially diverse 14C ages (Bao et al.,2016; Grifﬁth et al., 2010; Tesi et al., 2014; Wu et al., 2013), partly reﬂecting codeposition of OM from the terrestrial and marine biosphere.

©2019. American Geophysical Union.
All Rights Reserved.

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Lateral dispersal of sedimentary OM and associated hydrodynamic processes on continental shelves add
another temporal dimension (Bian et al., 2013; Li et al., 2016), further inﬂuencing 14C ages of sedimentary OC (Bao, van der Voort, Zhao, et al., 2018; Bao, Uchida, Zhao, et al., 2018; Bröder et al., 2018; Keil

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Figure 1. Sample locations in the Yangtze River, East China Sea, and Okinawa Trough (map modiﬁed from Oguri et al.,2003). The solid black line shows the P‐Line.

et al., 2004; Mollenhauer et al., 2007; Tesi et al., 2016). These processes in marginal seas can increase
14
C ages of OM by several millennia; the magnitude of aging depends on many factors such asdispersal distance, current velocity, and sediment grain size (Bao, Zhao, et al., 2019; Bao, Uchida,
Zhao, et al., 2018; Bröder et al., 2018). Due to complex and often temporally varying hydrodynamic
conditions, these processes can result in markedly spatial variability in sedimentary OC 14C inshallow marginal seas (Bao, Blattmann, et al., 2019). Translocation of sedimentary OM may occur
from the shelf to the deep ocean, where it may encounter differing hydrodynamic and depositional
regimes (Bao, Strasser, McNichol, et al., 2018; Blattmann et al., 2018; Hung et al., 2003; Hwang et al.,2010; Oguri et al., 2003; Zhu et al., 2006). This complex interplay between source inputs andtransport processes renders it challenging to deconvolve underlying carbon cycling, solely based on
bulk‐level information (incl., 14C) on sedimentary OM.
The East China Sea (ECS) forms an interface between the Yangtze River and Okinawa Trough, receiving
substantial inputs of both terrestrial and marine OM (Deng et al., 2006; Li et al., 2012; Wu et al.,2013; Zhu et al., 2013). This broad and shallow marginal sea is characterized by redistribution andremobilization of sedimentary OM (Bao et al., 2016; Deng et al., 2006; Li et al., 2016; Wu et al., 2013;
Zhu et al., 2006), and numerous studies have investigated regional changes in carbon biogeochemistry
and dynamics along shelf‐perpendicular transects (Figure 1, P‐Line; Iseki et al., 2003; Oguri et al.,
2003; Hung et al., 2003; Zhu et al., 2006). Prior studies have shown that OM in surface sediments along
the P‐Line primarily derives from marine sources as well as terrestrial materials discharged from the
Yangtze River (Deng et al., 2006; Zhu et al., 2006) and that OM can be ultimately exported to theadjacent Okinawa Trough (Iseki et al., 2003; Kao et al., 2003; Oguri et al., 2003). We have conducted
an extensive 14C survey of bulk surface sediments at the ECS (Bao et al., 2016); however, 14C‐centric
investigations of organic components within bulk sediments along such a typical river‐shelf‐deepBAO ET AL.

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ocean transect have not yet been reported. In particular, in‐depth examination of 14C age characteristics
of OM from “upstream” (Yangtze River) and “downstream” (Okinawa Trough) locations has not been
attempted so far.
Such a systematically detailed 14C investigation along the Yangtze River‐ECS‐Okinawa Trough transect
can disentangle the inﬂuences of source‐ and transport‐related factors on sedimentary OC content andcomposition. In this study, we applied ramped pyrolysis‐oxidation (RPO; Rosenheim et al., 2008;
Bianchi et al., 2015; Zigah et al., 2017; Bao, Strasser, McNichol, et al., 2018, Bao, McNichol,
Hemingway, et al., 2018, Bao, McNichol, McIntyre, et al., 2018) coupled with 14C analysis to suspended
particulate matter (SPM) of the Yangtze River, four surface sediment samples along a shelf‐perpendiculartransect at the ECS (P‐Line), and one surface sediment from the northern Okinawa Trough to assess anddecipher the cause(s) of compositional and age variability within the source‐to‐sink system on a regional
scale (Figure 1). In addition, we examined source‐diagnostic biomarker (n‐alkanoic acid) contents of
ECS surface sediments along the transect to further constrain the fate of terrestrial OM. Findings fromthis in‐depth assessment of underlying causes of OC 14C age variability along a river‐shelf‐deep oceantransect carries important implications for our understanding of carbon dynamics on and beyond
continental margins.

2. Sample Locations and Methods
2.1. Across‐Shelf Transect and Sample Locations
Approximately 47% of the sediments exported by the Yangtze River are deposited in the deltaic
area, with the remainder transported to the ECS shelf area (Du et al., 2016; Liu et al., 2006, 2007;
Milliman et al., 1985). Although the majority of the material escaping the delta (~32%) is transported
southward along the Min‐Zhe coast (Du et al., 2016; Liu et al., 2006), a substantial amount (~20%) of
terrestrial materials is dispersed offshore and across‐shelf (Oguri et al., 2003). Fine sediments and associated OM accumulating in the prodeltaic area are subject to intensive resuspension by hyrodynamicallydriven processes, and parts of these resuspended materials can be transported to the deep ocean alongacross‐shelf in winter (Oguri et al., 2003; Peng & Hu, 1999; Zhu et al., 2006). Substantial amountof coarse sediments deposits on the middle shelf under the control of tidal currents (Gao &Collins, 2014; Zhu & Chang, 2000). Additionally, sediments derived from the ECS shelf are accumulating in the Okinawa Trough, transported in the benthic layer during winter (Hoshika et al., 2003; Iseki
et al., 2003; Oguri et al., 2003). Across‐ECS shelf transect connecting to the deep ocean provides aregion‐scale OC source‐to‐sink system with a sharp contrast in hydrographic and depositional characteristics, compared to depositing environments of coastal mud belt along the ECS inner shelf (Bao, Zhao,
et al., 2019; Li et al., 2012). The former exerts more complex dynamics of sedimentation and ambiguous
sources of materials.
SPM from the Yangtze River was collected in July 2012 at Xuliujing (XLJ; 120.93°E, 31.78°N), ~100km upstream from the Yangtze River mounth (Figure 1). Detailed information about sample site andcollection methods was described in Wu et al. (2015). The seven ECS surface sediment (0–2 cm) samples
were collected using a box corer along the P‐Line from the prodelta to the upper slope on the R/V
Dongfanghong II in July–August 2013 (Figure 1). The samples are divided into three representative
groups by water depth: (i) prodeltaic sediment (P01), with water depths below 30 m andsurface sediments mainly consisting of silt and clay. In this regime, sedimentation rate is ~4 cm/year
and mixing layer depth is ~5–10 cm (Jia et al., 2018; Liu et al., 2006; Oguri et al., 2003; Su & Huh,
2002); (ii) middle‐shelf sediments (P02, P03, P05, and P07), with water depths from 30 to ~100 m,
mainly consisting of sands with low sedimentation rate (0.2–0.5 cm/year) and approximately 5‐cm mixing layer depth (Huh & Su, 1999; Oguri et al., 2003; Qiao et al., 2017); (iii) outer‐shelf and slope area
sediments (P09 and P11), with water depths from ~100 to 200 m, consisting of silt and ﬁner sandwith lower sedimentation rate (~0.1 cm/year; Huh & Su, 1999). The water depth of the Okinawa
Trough is generally greater than 800 m and underlying surface sediments consist of silt to clay, withthe extremely low sedimentation and less bioturbation based on excess 210Pb proﬁle in the Okinawa
Trough sediments (~0.1 cm/year; Li et al., 1996; Oguri et al., 2003). The surface sediment (0–1 cm,
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HR6) sample was collected using a multicorer in the northern Okinawa Trough area (water depth, 1,065m) on the R/V Hakuhu Maru in July 2013. All samples were then stored in the freezer on board
until analysis.
2.2. Ramped Pyrolysis and Oxidation
RPO coupled with 14C analysis was developed at the National Ocean Sciences Accelerator Mass Spectrometry(NOSAMS) facility, Woods Hole Oceanographic Institution (WHOI; Rosenheim et al., 2008; Zigah et al.,2017; Hemingway et al., 2017; Bao, Strasser, McNichol, et al., 2018; Bao, McNichol, Hemingway, et al.,2018; Bao, McNichol, McIntyre, et al., 2018). The RPO technique is able to examine 14C age distribution ofdifferent organic constituents within sedimentary OM as a function of their thermochemical stability.
During RPO, samples are exposed to a linear temperature gradient; simultaneous oxidation of thermal
decomposition products (as discrete temperature windows or fractions) yields CO2 that can be trappedand subsequently measured for 14C age. The thermogram ﬁngerprint of evolved CO2 and coupled 14C agesof thermally resolved OC components enables assessment of age variability within sedimentary OM (Bao,McNichol, Hemingway, et al., 2018).
In this case, RPO of the six samples, comprising Yangtze River SPM as well as P‐Line and northern Okinawa
Trough (SPM, P01, P02, P05, P07, and HR6) surface sediments, was performed at NOSAMS (Figures 2 and 3).
Freeze‐dried samples were weighed into combusted petri dishes. A beaker ﬁlled with 37% HCl was placed at
the bottom of a glass desiccator, and samples were placed on a ceramic tray above the acid. The desiccator was
evacuated, and the samples were fumigated at 60 °C for 72 hr to remove carbonate. The HCl was subsequently
replaced with a beaker containing NaOH pellets, and the dessicator was again evacuated and placed at 60°C,
for 72 hr in order to neutralize any excess acid (Bao, McNichol, Hemingway, et al., 2018). The fumigated samples were weighed (~200 mg/sample, n = 6) and loaded into a quartz reactor, and heated using a linear temperature program (5°C/min) from 170°C until a maximum of 915°C. Evolved volatile products (thermal
decomposition fractions [Tn]) were simultaneously oxidized and removed from the reactor using a carrier
gas mixture of O2 and He (~8% O2, 35 ml/min total ﬂow rate). A continuous record of evolved CO2 was
obtained via a ﬂow‐through infrared CO2 analyzer (Sable Systems International Inc., CA‐10a), before CO2
derived from thermally volatilized components was sequentially collected in ﬁve temperature windows(intervals; 170–320°C [T1], 320–391°C [T2], 391–486°C [T3]; 486–570°C [T4], and 570–915°C [T5]).
Exceptions include the T5 windows of P02 and P05, which were collected between 570–650°C and 570–
720°C, respectively, due to blocked gas ﬂow during the experiment, and the CO2 evolved from the 570 to
915°C interval in the P07 was sequentially collected into two parts: 570–829°C and 829–915°C. Resulting
CO2 samples were trapped into precombusted glass tubes with ~50 mg CuO and ~10 mg Ag granules andcombusted (525°C, 1 hr) as a ﬁnal gas puriﬁcation step at NOSAMS (Bao, McNichol, Hemingway, et al.,2018). The puriﬁed CO2 samples (n = 31) were measured for 14C ages using a mini radiocarbon dating
System (MICADAS) at ETH Zurich (Ruff et al., 2007). All 14C data are reported as 14C age (year before present[BP]), as deﬁned by Stuiver and Polach (1977).
2.3. Fatty Acid (n‐Alkanoic acid) Analysis
Freeze‐dried P‐Line sediments (P01‐P11, n = 7) were microwave‐extracted for 20 min at 100°C (MARS, CEM
Corporation) in 9:1 dichloromethane/methanol to yield corresponding total lipid extracts. Each total lipid
extract was then saponiﬁed with 0.5 g KOH in methanol plus 0.1‐ml Milli Q water for 2 hr at 70°C. NaCl
(10 ml, 100g/L) was added to the saponiﬁed extracts, and then they were back‐extracted using hexane (10ml × 3) to yield “neutral” fractions. Following addition of concentrated HCl (until pH 2), the remaining
liquids were then back‐extracted using 4:1 hexane/dichloromethane to yield “acid fractions”. The acid fractions were methylated to yield the corresponding fatty acid methyl esters (FAMEs) using a mixture ofmethanol/concentrated HCl (95:5, 70°C for 12 hr). The methylated products were back‐extracted using hexane (10 ml × 3), and following blow‐down under N2 gas, the FAMEs were puriﬁed by silica gel column chromatography (fully activated) overlain by Na2SO4 and sequential elution with 4‐ml hexane, 4‐ml
dichloromethane/hexane (2:1; containing FAMEs), and 40ml dichloromethane. The concentrations of
FAMEs in the samples with extra standard (FAMEs) were determined by gas chromatography with ﬂame
ionization detector.
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Figure 2. (a) The ramped pyrolysis‐oxidation thermogram comparison between suspended particulate matter (SPM;
brown) and P01 (yellow) samples. The CO2 concentrations are normalized by the mass of sediments loaded into the14
ramped pyrolysis‐oxidation instruments. (b) The C age comparison of thermal decomposition fractions (T1, T2, T3, T4,
14
and T5) between SPM and P01 samples. The arrows show the C age changes of corresponding thermal fractions from
SPM to P01.

3. Results and Discussion
3.1. Aged OC in the Yangtze River Prodelta
The Yangtze River, the largest river draining into the ECS, discharges ~110 Mt/year sediment (Deng et al.,2006; Qiao et al., 2017; Yang et al., 2015), including ~2.1 Mt/year petrogenic OC (fossil OC, 14C dead; Galyet al., 2015) and ~2.3 Mt/year terrestrial biogenic OC (Galy et al., 2015; Li et al., 2015). Although a substantial
fraction of terrestrial OC is remineralized within the delta (Deng et al., 2006; Zhao et al., 2018; Zhu et al.,2013), substantial amounts of OC are delivered into the ECS. The OC loading on Yangtze River SPM (OC:SA, approximately 0.5 ±0.1 C mg/m2; Wu et al., 2013) is higher than that of the inner shelf of the ECS(0.33 ± 0.11 C mg/m2, n = 12; Wu et al., 2013) and reported δ13C values for the former (e.g., < −24‰;
Wang et al., 2012) are lower than that of the latter (−22.1‰, n = 16; Wu et al., 2013). This increase in δ13C
value and the decrease in OC:SA from SPM to prodeltaic sediments may be interpreted as both remineralization of terrestrial OM and replacement by marine OM (Keil et al., 1997). In addition, such compositional
shifts between SPM and prodeltaic sediments have been used to estimate terrestrial OC burial efﬁciencies(Blair & Aller, 2012; Goñi et al., 2005; Keil et al., 1997; Wu et al., 2013).
However, we ﬁnd a decrease in Δ14C values (~ −110‰, Wang et al., 2012; ~ −200‰, Wu et al., 2018)from Yangtze River SPM to prodeltaic sediment at station P01 (−305‰; Bao et al., 2016), which is notconsistent with the estimation of (aged) terrigenous OC loss and replacement with younger marine OC.
Sedimentation rate and mixing layer depth in this prodeltaic area are high (~4 cm/year) and ~5–10 cm,
respectively (Jia et al., 2018; Liu et al., 2006; Oguri et al., 2003; Su & Huh, 2002). Bioturbation should
thus not be major cause for the decreasing in Δ14C values. We propose that three processes may bepotentially responsible for this carbon isotopic discord: (i) preferential remineralization of relatively
young terrestrial OC, (ii) replacement with relatively old marine OM, and (iii) OC aging during the lateral transport. In order to examine these possibilities, we compare the thermograms of corresponding
thermal decomposition fractions between SPM and P01 samples (Figure 2a). We ﬁnd a decrease inentire integrated thermogram area (i.e., overall CO2 yield), especially for higher temperature fractions(e.g., T3, T4, and T5; brown area, Figure 2a) between the river SPM and deltaic sediment, reﬂecting
the overall decrease in OC loadings presumably as a consequence of signiﬁcant remineralization of
OC in this dynamic regime. The OC contributing to the higher temperature fraction is considered to
be predominantly refractory OC and fossil OC (Bao, McNichol, Hemingway, et al., 2018; Rosenheim& Galy, 2012), suggesting that a signiﬁcant proportion of pre‐old OC (e.g., ≳4,000 years, based on agesof the T3–5, fractions of SPM; Figure 2b) is lost during translocation of sedimentary OM from river todelta. These results are consistent with the observations of previous studies (Bao et al., 2016; Wu
et al., 2013). Our results support the possibility of remineralization of both young and old terrestrial
OC. Overall, most of the OC loss and bulk‐level 14C depletion from SPM to prodeltaic area areaccounted for by degradation of relatively younger (compared with remaining old OC) but pre‐old(>4,000 years) terrestrial OC.
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Figure 3. (a) Thermograms of OM from P01, P02, P05, P07, and HR6; inserts in P02 and P07 show the same scale of the y axis (mass‐normalized CO2 [ppm/mg]) as
14
other samples. (b) The C age variability among thermal windows along the across‐shelf transects; the arrows show the general trends. Note that the highest
temperature intervals of P02 and P05 were 570–650°C and 570–720°C, respectively. There was incomplete collection of CO2 due to blocked gas ﬂow during the1414experiments. The C age of T5 fraction in P07 sample is calculated based on the C ages and amounts of two sub‐intervals CO2 for 570–829°C and 829–915°C.

Compared with refractory OC, labile OC tends to decompose at lower temperatures (Bao, McNichol,
Hemingway, et al., 2018; Bao, McNichol, McIntyre, et al., 2018; Capel et al., 2005, 2006; Hemingway
et al., 2017). In the low‐temperature window (e.g., T1), the CO2 yield in the thermogram of the prodelta(P01) sample is slightly larger than for the corresponding fraction of river SPM (Figure 2a). This may
suggest addition (loading) of labile OC, which decomposes at lower temperatures. Nevertheless, the corresponding 14C age of the T1 fraction in sample P01 (2005 ±84 year BP) is slightly older than that of
SPM (1,560 ± 74 year B; Figure 2b). The radiocarbon age of dissolved inorganic carbon in the
Yangtze River estuary is relatively young, ranging from modern to 1,380 ±25 year BP (Wang et al.,2016). These various lines of evidence suggest that the older OC age (lower 14C value) of prodeltaic sediment relative to SPM is not mainly due to addition of pre‐old marine OM.
Recent studies have revealed signiﬁcant aging of sedimentary OC due to its prolonged lateral transport (~4–6
year per kilometer for ﬁner [< 63 μm] sediments; Bröder et al., 2018; Bao, Uchida, Zhao, et al., 2018; Bao,Zhao, et al., 2019). Hydrodynamic processes have been attributed for widespread OC aging observed in marginal sea systems globally, regardless of carbon source (Bao, van der Voort, Zhao, et al., 2018, reference
therein). The XLJ SPM sampling location is ~150 km away from P01 location. Station XLJ in the river isstrongly tidally inﬂuenced; the sedimentary OM transport across the XLJ to P01 locations may be subject
bi‐directional ﬂows depending on in‐situ hydrology and tidal forcing (Zhang et al., 2007, 2017). This could
contribute to aging during lateral transport as a consequence of sedimentary OM sloshing transport acrossthe typical tide‐dominated delta. Given sediment dynamics and associated hydrodynamic processes acrossthe river‐delta interface, it seems that aging of some organic components may occur due to the lateral transport. Overall, we infer that a combination of preferential removal of relatively younger terrestrial OM andhydrodynamically driven aging associated with lateral transport may be responsible for the increased ageof sedimentary OM depositing in the prodeltaic area.
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Figure 4. Relationships (a) between OC% and mineral surface area (SA) and (b) between long‐chain C24+26+28 FAs
14(LCFA) loadings (normalized to SA) and bulk OC C values for P‐Line sediment samples.

3.2. Aged OC Depositing Along the P‐Line in the ECS
In general, the OC content (OC %) of ECS shelf sediments is related to mineral surface area (SA; Wu et al.,2013; Bao, van der Voort, Zhao, et al., 2018; Figure 4a). Thermograms of the four representative P‐Line samples (P01, P02, P05, and P07; Figure 3a) resulted from RPO analyses are distinct, implying that organic constituents comprising each sample differ in both relative proportions and absolute abundances. The
differences in OM content and composition inﬂuence their corresponding bulk 14C ages. The relatively
old 14C ages of OC in ECS shelf surface sediments mainly attribute to inputs of pre‐old terrestrial OM(Wu et al., 2013).
In order to assess the preservation of terrestrial OC and its impact on 14C age, we examine the abundances ofstraight‐chain (n‐) fatty acids (FAs) in the P‐Line sediments. Concentrations and distributions of n‐FA
homologues systematically vary along across the P‐Line samples (Figure 5). The C16 FA is the most abundant compound, with maximum and minimum concentrations of 8.4 and 0.4 μg/gdw from prodeltaic(P01) and middle shelf (P07) samples, respectively. The concentrations of long‐chain C24+26+28 FAs(LCFAs), which are considered to mainly derive from terrestrial higher plants (Eglinton & Hamilton,1967), are the highest in prodeltaic P01 sample, whereas the concentrations of LCFAs in middle‐shelf samples (P05 and P07) are the lowest. The former are ﬁner‐grained sediments with higher mineral SA comparedwith the latter, likely suggesting that association with mineral surfaces may be an important factor in controlling the terrestrial OC preservation in sediments along the P‐Line. With the exception of the river‐proximal P01 sample, SA‐normalized LCFA concentrations (i.e., loadings) exhibit a positive relationshipwith bulk OM 14C values (Figure 4b). This suggests that proportion of (pre‐old) terrestrial OM is one of
the main reasons inﬂuencing on OC 14C ages in ECS shelf sediments, and these bulk 14C ages are thus constrained by similar mechanisms.
The abundance and composition of terrestrial OC in surface sediments are related not only to mineral SA but
also to speciﬁc hydrodynamic processes associated with its across‐shelf transport. The abundance of terrestrial OC has been linked to lateral transport time during pre‐depositional processes of sediment remobilization and redistribution (Bao et al., 2016; Bao, Blattmann, et al., 2019; Bao, Uchida, Zhao, et al., 2018; Bao,Zhao, et al., 2019; Bröder et al., 2018; Keil et al., 2004). Since sedimentary OM is heterogeneous, OC constituents may experience different predepositional histories, thus inﬂuencing overall (bulk) OC 14C ages in
sediment. We ﬁnd that the 14C ages of the different thermal windows generally increase with increasing temperature (from T1 to T5), with a large range in 14C ages between the lowest (T1, 692 year BP) and highest (T5,16149 year BP) temperature intervals (Figure 3b and Table S2). 14C ages of T1 fractions decrease (i.e.,
increase in 14C contents) along the seaward transect (red bars, Figure 3b). This likely reﬂects a combinationof less resuspension inﬂuence (Bao, Blattmann, et al., 2019), and aged OC removal from labile fractions during lateral transport coupled with addition of young OM derived from vertical export of surface ocean productivity. The latter is consistent with the higher concentrations of short‐chain (C14, C16, and C18) FA in theouter shelf and slope settings (P09 and P11; Figure 5) that receive hemipelagic sedimentation (Bi et al., 2018;
Li et al., 2016; Oguri et al., 2003; Qiao et al., 2017; Yang et al., 2007).

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Figure 5. Concentrations of solvent‐extractable C14‐C34 fatty acids (μg/g dry weight) in surface sediments (P01, P02, P03 P05, P07, P09, and P11) from the P‐line
transect in the East China Sea.

In contrast to the low‐temperature windows, 14C ages of higher temperature windows (e.g., T4 and T5) generally increase along this transect (Figure 3b). Middle‐shelf sediments (P02, P03, P05, and P07) are coarser,
and corresponding LCFA concentrations are very low, implying intensive degradation before and following
deposition. The remaining OC within these coarser sediments is therefore likely to be relatively refractorycompared with that associated with ﬁner particles (Bao, McNichol, Hemingway, et al., 2018; Bao,
McNichol, McIntyre, et al., 2018). Nevertheless, the P‐Line sediments do not exhibit systematically increasing
grain size with increasing across‐margin distance. The mode of benthic transport may inﬂuence ages ofrefractory OM (e.g., near‐bottom nepheloid layer transport; Bao, Blattmann, et al., 2019). The sediment transport seaward in the bottom layer is observed seasonally (Hoshika et al., 2003; Oguri et al., 2003; Zhu et al.,2006). The overall increasing age of higher temperature fractions (refractory OC) associated with lateraltransport along the P‐Line may reﬂect the hydrodynamic regime, although we cannot completely exclude
the possibility of aged OC from different sources (e.g., old Yellow River (Saito & Yang, 1995) and relict sediments on the shelf (Deng et al., 2006)) inﬂuencing the ages of refractory fractions. To summarize, the contrasting 14C age trends between the low‐ and high‐temperature windows along the P‐Line thus suggestthat different transport modes inﬂuence preservation, distribution, and age of sedimentary OM, highlighting
the important control of hydrodynamic processes on the fate of OM in the marginal seas.
3.3. Aged OC in the Okinawa TroughOM produced and travelling on the ECS shelf can be exported down‐slope to the Okinawa Trough (Iseki
et al., 2003; Oguri et al., 2003). It has been estimated that at least 0.17 mg C cm−2 year−1 of sedimentary
OM is delivered by lateral transport and accumulates in the trough, compared with 0.25 mg C cm‐2 year−1
supplied via vertical export (Oguri et al., 2003). While the former may derive from several potential sources,
including the Yellow River (Katayama & Watanabe, 2003), the old Yellow River (Yuan et al., 2008; Zhao
et al., 2019), and Taiwan island (Kao et al., 2003, 2008; Li et al., 2018), some of OC deposited in the
Okinawa Trough must originate from the adjacent ECS shelf area (Dou et al., 2010a, 2010b; Honda et al.,
2000; Iseki et al., 2003; Oguri et al., 2003).

Figure 6. Comparison between T1 (red bar) and T5 (black bar) thermal fractions along the land‐ocean transect. Due to the incomplete collection of
evolved CO2 for T5 fractions from P02 and P05, the two samples are notpresented.

BAO ET AL.

The 14C ages of sedimentary OM in the surface sediment of Okinawa
Trough have not, to our knowledge, been investigated in detail (Honda
et al., 2000). Our RPO investigation reveals a large range of 14C ages
among thermal fractions of the surface sediment investigated (HR6;
Figure 3b). We ﬁnd that the highest temperature window exhibits a very
old age (T5 fraction: 14,979 ±170 year BP), while its bulk OC 14C is relatively young (2,264 ±82 year BP; Bao et al., 2016). We also ﬁnd that thecorresponding 14C age of T1 fraction in HR6 sediment is the youngest
among those investigated in this study (594 ±75 year BP; Figure 3b). As
a result, a large 14C age heterogeneity (corresponding to a 14,385 ±245
years, 14C age offset between minimum and maximum temperature windows) is found in the Okinawa Trough. Notably, the extent of this heterogeneity is larger than that observed from RPO analysis of hadal zone,
Japan Trench (>7,500 m) sediments (~4,000 years; Bao, Strasser,
McNichol, et al., 2018), suggesting complex OM compositions in the
Okinawa Trough. Figure 6 reveals that the spread in 14C ages among
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Figure 7. Conceptual schematics showing four scenarios to explain potential origin of increases aged sedimentary organic matter, and their potential manifestationin ramped pyrolysis‐oxidation thermograms. (a) fossil organic carbon (OC) input, (b) selective degradation of younger OC, (c) hydrodynamic sorting, and (d)protracted lateral transport.

RPO fractions increases along the river‐shelf‐deep ocean transect. We thus argue that this ampliﬁed 14C
heterogeneity in the Okinawa Trough is due to a combination of varying hydrodynamic forcing anddifferent OM inputs (e.g., pre‐old OC derived from the ECS shelf/slope; marine OM produced in overlying
water column; Bi et al., 2018; and potential aerosols input, Yu et al., 2018; Bao, Niggemann, Luo, et al., 2018).
During prolonged lateral transport, OM may experience 14C aging as a consequence of both selective degradation of relatively labile and young OM, and lateral transport time. Together, these processes manifest
themselves as an increase in the proportion and 14C age of high temperature (T5) fractions corresponding
to refractory OM (top black arrows, Figure 6). In contrast, the lowest temperature fraction (T1) fraction
decreases in age, due primarily to addition of recently synthesized and vertically supplied marine OM as wellas less‐resuspension. Based on the comparison of thermogram of HR6 with those from the P‐Line(Figure 3a), we suggest that pre‐old and refractory sedimentary OM accumulates in the Okinawa Trough.
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Consequently, the increase of aged OM in marginal sea and trough sediments largely depends on its relative abundance and the 14C ages of refractory fractions. Based on our coupled RPO‐14C investigations, we
propose four potential scenarios that may result in the observed aged sedimentary OM along the transectfrom the Yangtze River mouth to the Okinawa Trough, and over continental margins, in general. The
manner in which these different scenarios may manifest themselves in the RPO thermograms is depicted
in Figure 7:
1. Fossil OM: Fossil OC would manifest itself in the higher temperature thermal window from RPO of sedimentary OM (Bao, van der Voort, Zhao, et al., 2018; Kao et al., 2008; Rosenheim & Galy, 2012; Wu et al.,2013). Because of its highly refractory and 14C‐dead characteristics, the magnitude and age of this component corresponding to this largely unreactive material would be anticipated to increase, given fossil
OM input (Figure 7a).
2. Selective degradation of younger OM: Selective degradation of OM in marine sediments may be inﬂuenced by several factors including lateral oxygen exposure time, degree, and mode of association withmineral surfaces, and hydrodynamic regime (Arnarson & Keil, 2007; Bao, Zhao, et al., 2019; Bröder
et al., 2018; Keil et al., 2004; Zonneveld et al., 2010). In general, labile OC is preferentially removed
and this OM tends to decompose and manifest itself in CO2 evolved at lower RPO temperatures (Bao,McNichol, Hemingway, et al., 2018; Capel et al., 2005, 2006). This removal of labile OC during lateraltransport would result in a relative increase in the proportion of refractory OC contributing to the thermogram (Figure 7b).
3. Hydrodynamic sorting: Speciﬁc grain size has a greater propensity for resuspension and redistribution
than others during lateral transport (McCave & Hall, 2006), leading to sediment sorting and attendantchanges in associated OM. For example, ﬁner‐grained sediments hosting younger OM may be preferentially winnowed with older OC retained on the outer shelf of the ECS (Bao, van der Voort, Zhao, et al.,2018), leading to apparent aging of remaining OC (Figure 7c).
4. Protracted lateral transport: During lateral transport, OM that is vulnerable for degradation is preferentially removed, while residual OM persists, the latter is presumably closely associated with mineral surfaces (or insides) (Arnarson & Keil, 2007). These OM‐mineral associations may further strengthen as aconsequence of protracted engagement (Bao, McNichol, McIntyre, et al., 2018), thereby enhancing OM
thermochemical‐stability and resulting in a shift of the corresponding thermogram peak to higher temperatures (Figure 7d; Bao, Strasser, McNichol, et al., 2018). More importantly, across‐ and along‐shelf lateral transport times may range from hundreds to thousands of years, depending on transport distanceand other factors (Bao, Uchida, Zhao, et al., 2018; Bao, Zhao, et al., 2019). The time component of protracted lateral transport would cause an increase in OC 14C age as a consequence of radioactive decay.
The transport‐related aging (or decrease in 14C content) of OC requires careful consideration in assessment of source apportionment of sedimentary OC calculated using 14C mass balance approaches (Bao,Uchida, Zhao, et al., 2018).

4. Conclusions
Although the present analyses are mainly based on RPO and 14C measurements of a limited number of sediments recovered along the typical river‐shelf‐deep ocean transect, they serve to assess the origin of aged sedimentary OM and constraint potentially which scenario is the most important for the fate of OM depositing indifferent marginal sea environments. We think that this selective degradation of younger OC processes may
be main reason for aged OM observed in this interface between the Yangtze River and ECS. Contrastingly,
coarser sediments on the middle shelf of ECS (mean grain size: ≳200 μm) compared with ﬁner deltaic sediments that are subject to hydrodynamic sorting, indirectly causing different carbon source proportions in
sediments. The hydrodynamic sorting is considered as the most direct and important cause for the contrasting change of 14C ages on the shelf compared with that in deltaic area. Fossil OC and OC derived from the
ECS shelf both could be carbon source for contemporary sediments in the Okinawa Trough. Wherever thesources of aged OM depositing in the trough are from, nevertheless, they must be subject to long‐distancetransport. The hydrodynamically driven processes inﬂuencing in age should be seriously considered, in particular, for interpretation of millennial‐scale paleoceanographic and paleoclimate signals by virtue oforganic geochemical proxies in the Okinawa Trough.
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Overall, this investigation of 14C age distribution and heterogeneity in sedimentary OM extending from the
Yangtze River mouth to the northern Okinawa Trough provides new insights into the cause(s) of compositional and age variability within the region‐scale source‐to‐sink system. We ﬁnd that apparent aging OM
along the across‐shelf transect are a consequence of a combination of source variations, selective degradation, and hydrodynamically driven processes (sorting and transport related aging). These causes, which
can be closely interlinked, lead to substantial OC 14C age heterogeneity within sediments, in particular, in
the Okinawa Trough. The conceptual modes we propose serve as a framework for interpretation of potential
causes of aged OC based coupled RPO‐14C data.

Acknowledgments
This study was supported by Doc.
Mobility Fellowship (P1EZP2_159064;
R. B.) from the Swiss National Science
Foundation (SNSF). This study was also
supported by SNF “CAPS‐LOCK”
project 200021_140850 (T. I. E.), by the
National Natural Science Foundation ofChina (NSFC; grants 41520104009 and41630966, M. Z.), and by the “111”project (B13030). We are grateful for
support of the NOSAMS staff in theexecution of this project. We also
appreciate the assistance from
Yushuang Zhang (Ocean University of
China) at NOSAMS and members of theLaboratory for Ion Beam Physics at
ETH Zurich for AMS measurements.
We acknowledge Lei Xing, Haidong
Zhang, Guodong Song, Meng Yu,
Yonghao Jia, and Shanshan Duan
(Ocean University of China) for sampling assistance on the cruises.
Assistance at sea by the crews of R/V
Dongfanghong II and R/V Hakuhu
Maru is also acknowledged. Readers
can access or ﬁnd the data from ﬁgures
and tables in the supporting
information.

BAO ET AL.

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