Front. Mar. Sci. Frontiers in Marine Science Front. Mar. Sci. 2296-7745 Frontiers Media S.A. 10.3389/fmars.2024.1469283 Marine Science Original Research Manganese mineralization constrained by redox conditions in the Cryogenian Nanhua Basin, South China and its implications for nitrogen and carbon cycling Wang Ping 1 * Wang Jian 1 Du Yuansheng 2 Yu Wenchao 2 Zhou Qi 3 Tian Li 4 Yuan Liangjun 5 Pan Wen 5 Wei Wei 2 Qin Yongjun 3 Ma Zhixin 3 6 1 School of Resources and Environment, Henan Polytechnic University, Jiaozuo, China 2 School of Earth Sciences, China University of Geosciences, Wuhan, China 3 Engineering Technology Innovation Center of Mineral Resources Explorations in Bedrock Zones, Ministry of Natural Resources, Guiyang, China 4 State Key Laboratory of Marine Environmental Science, Xiamen University, Xiamen, China 5 103 Geological Party, Guizhou Bureau of Geology and Mineral Exploration and Development, Tongren, China 6 Chengdu Center, China Geological Survey, Chengdu, China

Edited by: Fei Li, Southwest Petroleum University, China

Reviewed by: Zhang Yi, Chongqing University, China

Chunhua Shi, Guizhou University, China

*Correspondence: Ping Wang, wangping_2016@163.com

23 09 2024 2024 11 1469283 23 07 2024 30 08 2024 Copyright © 2024 Wang, Wang, Du, Yu, Zhou, Tian, Yuan, Pan, Wei, Qin and Ma 2024 Wang, Wang, Du, Yu, Zhou, Tian, Yuan, Pan, Wei, Qin and Ma

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The Nanhua Basin of South China recorded complete Cryogenian stratigraphic sequence from the Sturtian Glaciation (~717–660 Ma) to the Marinoan Glaciation (~654–635 Ma). The interglacial Datangpo Fm in the Nanhua Basin is divided into two members, and the first member consists of the Mn-carbonate unit and the overlying black shale unit, containing a series of large and superlarge manganese deposits. The metallogenic process of manganese deposits is not clear, and the Mn-carbonates formed through the precursor of Mn-oxide/oxyhydroxide reduction or directly precipitated from an anoxic water column. Moreover, the redox conditions in the deep Nanhua Basin during the precipitation of manganese deposits are also controversial. In this study, the high-resolution nitrogen contents (TN), isotope compositions, carbon isotope compositions of organic and inorganic matter from the first member of the Datangpo Fm are analyzed. The δ15N values of the Mn-carbonate unit (+1.53‰ to +5.26‰, mean +3.36‰) are higher than those of the overlying black shale unit (−3.74‰ to +3.54‰, mean +0.89‰). The Mn contents show a negative relationship with TN but a positive relationship with δ15N in the Mn-carbonate unit, implying that the formation of Mn-carbonates is related to redox variations. The relatively higher δ15N values in the Mn-carbonate unit indicated oxic conditions, and NH4 +can be released and partially oxidized during the mineralization of organic matter, resulting in the residual 15N-enriched NH4 + being transferred into clay minerals. Meanwhile, the lower δ15N values in the black shale unit indicated anoxic conditions, which recorded primary N isotope signals. The Mn-carbonate unit is characterized by negative δ13Ccarb values (−11.17‰ to −5.22‰, mean −8.30‰), which show a positive relationship with δ13Corg, but a negative relationship with Mn contents, implying that the negative δ13Ccarb excursions were related to the organic matter degradation during Mn-carbonate formation. The findings of this study indicated that the metallogenesis of manganese deposits in the Cryogenian Nanhua Basin was constrained mainly by the oxic interval in the deep basin. The nitrogen and carbon cycling process can provide new insights into geochemical cycling after the Sturtian Glaciation.

 Mn-carbonate black shale nitrogen isotope carbon isotope negative carbon isotope excursions metallogenesis 42202111 National Natural Science Foundation of China10.13039/501100001809 Key Scientific Research Project of Colleges and Universities in Henan Province10.13039/501100013066 section-in-acceptance Marine Biogeochemistry Introduction

The Earth experienced two global glaciation events in the Neoproterozoic Era (~1,000–542 Ma), i.e., the older Sturtian Glaciation (~717–660 Ma) and the younger Marinoan Glaciation (~654–635 Ma) (Kirschvink, 1992; Hoffman et al., 1998; Hoffman and Schrag, 2002). Sedimentary manganese deposits precipitated widely during this period in Brazil, Namibia, India, and South China (Roy, 2006; Yu et al., 2016). Mn was preserved as Mn-carbonates in India and South China (Roy et al., 1990; Gutzmer and Beukes, 1998; Yu et al., 2016; Zhou et al., 2016), but as Mn-oxides interbedded with banded iron formations (BIFs) in Namibia and Brazil (Bühn et al., 1992; Klein and Ladeira, 2004; Cabral et al., 2011). A series of large–superlarge manganese deposits were discovered in the post-Sturtian deep Nanhua Basin of South China (Zhou et al., 2016, 2022).

It is generally considered that the metallogenic processes of the manganese deposits in the Cryogenian Nanhua Basin of South China experienced two stages (Yu et al., 2016, 2017; Wu et al., 2016; Xiao et al., 2017). During Stage I, the dissolved Mn2+ sourced mainly from hydrothermal activity (Wu et al., 2016; Yu et al., 2016) were oxidized to Mn-oxides/oxyhydroxides under oxic conditions and then sank to organic matter-enriched sediments. During Stage II, the insoluble Mn-oxides/oxyhydroxides were reduced to Mn2+ in porewater during the organic matter mineralization, which subsequently reacted with HCO3 − and were preserved as Mn-carbonates during the sedimentary-early diagenetic process (2MnO2 + CH2O + HCO3 − → 2MnCO3 + H2O + OH−). The organic matter acted as electron acceptor during the reduction of Mn-oxides/oxyhydroxides and can be oxidized to 13C-depleted HCO3 −. Both stages were mediated by microbial activities (Roy, 2006; Yu et al., 2016, 2019). The oxidation of dissolved Mn2+ was mediated by enzymatic multicopper oxidase processes associated with autotrophic microbial activity under oxic conditions (Tebo et al., 2004; Morgan, 2005; Yu et al., 2019), whereas the Mn-oxide/oxyhydroxide reduction to Mn2+ in porewater was mediated by heterotrophic microbes under suboxic conditions (Yu et al., 2019), similar to the Jurassic Úrkút manganese deposits in Hungary (Polgári et al., 2012a, 2012b). However, an alternative metallogenic process of the manganese deposits was recently proposed, during which the Mn-carbonates were directly precipitated from the anoxic water column in the Cryogenian Nanhua Basin (Ai et al., 2023).

The redox conditions of the post-Sturtian Nanhua Basin are still controversial. Some studies suggested that the deep Nanhua Basin was anoxic, after which the oxygenation expanded (e.g., Cheng et al., 2021; Wu et al., 2024). However, other studies have shown that the deep Nanhua Basin experienced episodic ventilation, similar to the Baltic Sea (Yu et al., 2016; Xiao et al., 2017; Ai et al., 2021). Furthermore, the relationship between redox conditions and the metallogenic process of sedimentary manganese deposits in the Cryogenian Nanhua Basin still needs to be further studied. The negative carbon isotope excursions of the Mn-carbonate unit of the manganese deposits in the Cryogenian Nanhua Basin were reported, ranging between −5‰ and −12‰ (mean ca. −8‰) (e.g., Li et al., 1999; Zhou et al., 2007; Chen et al., 2008; Wu et al., 2016; Qu et al., 2018; Zhu et al., 2019; Pei et al., 2020; Tan et al., 2021). The negative δ13Ccarb excursions might be related to organic matter, which can provide 13C-depleted carbon (Li et al., 1999; Chen et al., 2008; Wu et al., 2016; Qu et al., 2018; Zhu et al., 2019; Dong et al., 2023). However, how the 13C-depleted organic matter affected the carbon isotope compositions of the Mn-bearing sediments and whether the negative δ13Ccarb excursions are related to the formation of Mn-carbonates remain unclear.

This study focuses on the drillcore ZK2115, which is located in the Gaodi Manganese Deposit, eastern Guizhou Province. The high-resolution nitrogen and carbon geochemical data are analyzed for the Mn-carbonate unit and the overlying black shale unit of the post-Sturtian Datangpo Fm. Combined with the previously reported total organic carbon (TOC) and Mn contents in the study units, the redox proxy-δ15N values suggested that the deep basin was oxic during the precipitation of the Mn-carbonate unit, which facilitated the metallogenic process of the manganese deposits. The Mn-carbonate formation experienced the Mn2+ oxidation and reduction stages, leading to the negative δ13Ccarb excursions in the basal Datangpo Fm. Carbon and nitrogen cycling in the Cryogenian is reconstructed, which can also provide new insights for the global N–C cycling throughout Earth’s history.

 Geological background

The Nanhua Basin developed as a rift basin between the Yangtze Block and Cathaysia Block during the breakup of the Rodinia supercontinent in Neoproterozoic (Dalziel, 1991; Hoffman, 1991; Moores, 1991; Li et al., 2008; Wang and Pan, 2009) ( Figures 1A, B ). The Nanhua Rift Basin consists of Wuling and Xuefeng secondary rift basins and the Tianzhu–Huitong Uplift between them. The Wuling Secondary Rift Basin consists of a series of NE–SE-trending grabens and horsts (Zhou et al., 2016, 2022), and a series of manganese deposits precipitated in the small grabens of the rift basin in a similar spreading direction ( Figure 1C ).

(A) Tectonic units of China. (B) Structure of the Nanhua Rift Basin on the southeast margin of the Yangtze Block (Zhou et al., 2016). (C) Distribution of Datangpo-type manganese deposits in the Guizhou–Hunan–Chongqing adjacent area (modified from Zhou et al., 2016, 2022). The study drillcore ZK2115 is marked by red stars.

The Nanhua Basin recorded complete Cryogenian stratigraphic sequence, including the Tiesi’ao Fm, Datangpo Fm, and Nantuo Fm ( Figure 2A ). The Tiesi’ao and Nantuo formations recorded glaciomarine sediments during the Sturtian and Marinaon glaciations, while the Datangpo Fm recorded the interglacial sediments between the two global glaciations. The Datangpo Fm is subdivided into two members, the first member consists of the Mn-carbonate unit and the overlying black shale unit, while the second member consists of gray siltstones. The manganese deposits discovered in the Cryogenian Nanhua Basin are called “Datangpo-type” manganese deposits. Moreover, the coeval cap carbonates precipitated in the horsts of the Nanhua Basin (Yu et al., 2017, 2020). There are two types of manganese ores in the “Datangpo-type” manganese deposits, i.e., banded ores ( Figure 2B ) and massive ores ( Figure 2C ). In the “Datangpo-type” manganese deposits, the thickness of the Mn-carbonate unit decreased from the center of the basin to the edge, whereas the ore types changed from massive ores to banded ores, accompanied by the decreasing Mn contents (Zhou et al., 2013, 2022). The study drillcore ZK2115 is located in the Gaodi Manganese Deposit ( Figure 1C ).

(A) Cryogenian stratigraphic sequence of drillcore ZK2115 in the Nanhua Basin of South China. Two ore types of the “Datangpo-type” manganese deposits precipitated in the basal Datangpo Fm, i.e., banded ores (B) and massive ores (C).

The termination of the Sturtian Glaciation was globally synchronous and limited to ca. 660 Ma through zircon U-Pb and Re-Os dating (e.g., Rooney et al., 2015; Hoffman et al., 2017). The similar radiometric ages were also reported in South China. For example, the uppermost Tiesi’ao Fm yielded a Re-Os age of 660.6 ± 3.9 Ma (Rooney et al., 2020). The Mn-carbonate unit of the Datangpo Fm yielded zircon U-Pb ages of ca. 660 Ma through LA-ICP-MS (Yu et al., 2017; Ma et al., 2023), SIMS (Wang et al., 2019a), ID-TIMS (Zhou et al., 2004), CA-ID-TIMS (Rooney et al., 2020; Zhou et al., 2020), and SHRIMP (Yin et al., 2006), with a Re-Os age of 660.6 ± 7.5 Ma (Pei et al., 2017). Moreover, the coeval post-Sturtian cap carbonates in South China also yielded a similar zircon U-Pb age of 658.8 ± 0.5 Ma via CA-ID-TIMS (Zhou et al., 2019). The geochronological lines of evidence can also be used to constrain the formation age of the “Datangpo-type” manganese deposits.

 Samples and methods

The present study focuses on the drillcore ZK2115 ( Figure 1 ). A total of 38 samples were collected from the first member of the Datangpo Fm, including 24 samples from the Mn-carbonate unit (~11 m) and 14 samples from the black shale unit (~30 m).

The collected fresh samples avoiding veins were cleaned and crushed to ~200 mesh before geochemical analyses. The TN contents, inorganic carbon and oxygen isotope, and organic carbon isotope compositions were conducted at the State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences (Wuhan).

The TN contents were analyzed in an Elementar Vario MACRO CUBE element analyzer, and the analytical precisions are better than 0.02%. The inorganic carbon and oxygen isotope compositions were analyzed using a MAT253 isotope ratio mass spectrometer. The results are expressed in delta notation as per mil (‰) deviations relative to Vienna Pee Dee Belemnite (VPDB) standard (δ13C = [(13C/12C)sample/(13C/12C)VPDB − 1] * 1,000). The analytical precisions are better than 0.1‰ based on two laboratory standards (GBW04416 and GBW04417).

Before the nitrogen and organic carbon isotope analyses, the carbonate portions should be removed. The powder samples were treated with 4 M hydrochloric acid until the carbonates were completely reacted. Then, the residues were rinsed by deionized water for several times until pH tests gave a near-neutral value (≥6.0). The samples were then centrifuged and dried in the oven at 50°C. The carbonate-free samples were analyzed using an EA+MAT253 isotope ratio mass spectrometer. The results are also expressed in delta notation as per mil (‰) deviations relative to the VPDB standard (δ13C = [(13C/12C)sample/(13C/12C)VPDB − 1] * 1,000). The analytical precisions are better than 0.06‰, and the analysis results are based on three laboratory standards (GBW04407, GBW04408, and ACET).

The carbonate-free δ15N values of the study samples were analyzed in EA+IRMS (isotope ratio mass spectrometry; IsoPrime 100) at the State Key Laboratory of Marine Environmental Science, Xiamen University. The results are reported using standard delta notation as deviations (δ15N = [(15N/14N)sample/(15N/14N)standard − 1] * 1,000); the standard is atmospheric N2 with a δ15N value of 0‰. The analytical precisions are better than 0.1‰ based on laboratory standards (USGS40, GUGS41, and IAEA-600).

 Results

All geochemical data for the Mn-carbonate unit and the black shale unit are given in Table 1 . The TN contents range from 0.02% to 0.12% (mean 0.06%) in the Mn-carbonate unit and from 0.07% to 0.10% (mean 0.08%) in the black shale unit ( Figure 3 ). The δ15N values decrease from the Mn-carbonate unit (+1.53‰ to +5.26‰, mean +3.36‰) to the overlying black shale unit (−3.74‰ to +3.54‰, mean +0.89‰) ( Figure 3 ). The δ13Corg values vary from −33.61‰ to −31.82‰ (mean −32.84‰) in the Mn-carbonate unit and from −31.92‰ to −30.55‰ (mean −31.20‰) in the black shale unit ( Figure 3 ). Meanwhile, the δ13Ccarb values range between −11.17‰ and −5.22‰ (mean −8.30‰) in the Mn-carbonate unit, while the δ18O values range between −10.14‰ and −4.81‰ (mean −8.57‰) ( Figure 3 ). The C/N values range between 14.9 and 128.6 (mean 56.0) in the Mn-carbonate unit, which are higher than the black shale unit (15.8 to 44.2, mean 25.8).

Geochemical data of the drillcore ZK2115 in Gaodi Deposit, Guizhou Province.

Formation Sample no. Depth TN δ15N δ13Ccarb δ18O δ13Corg TOC K2O Mn C/N
(m) (%) (‰) (‰) (‰) (‰) (%) (%) (%)
Datangpo Fm ZK2115-H49 1,597.40 0.07 3.54 −30.80 1.0 3.2 0.2 16.9
Black shale unit ZK2115-H47 1,599.40 0.08 3.52 −30.55 1.2 3.0 0.2 17.7
ZK2115-H45 1,601.40 0.08 0.23 −30.91 1.3 2.9 0.1 20.8
ZK2115-H43 1,603.40 0.09 −3.74 −30.97 1.9 3.3 0.1 25.6
ZK2115-H41 1,605.40 0.08 1.24 −30.92 2.9 3.1 0.2 41.8
ZK2115-H39 1,607.40 0.08 1.45 −31.11 3.1 3.3 0.4 44.2
ZK2115-H35 1,611.40 0.08 1.85 −31.92 2.7 3.5 0.5 39.5
ZK2115-H33 1,613.40 0.07 0.53 −31.21 1.9 4.0 0.3 30.9
ZK2115-H31 1,615.40 0.10 1.54 −31.22 1.3 4.7 0.2 15.8
ZK2115-H29 1,617.40 0.08 1.30 −31.64 1.7 4.1 0.3 24.4
ZK2115-H27 1,619.40 0.10 1.75 −31.33 1.7 4.1 0.4 20.0
ZK2115-H25 1,621.40 0.08 −0.61 −31.70 1.6 4.0 0.2 22.0
ZK2115-H23 1,623.40 0.09 1.33 −31.26 1.8 4.4 0.2 22.6
ZK2115-H21 1,625.40 0.09 −1.54 1.6 4.4 0.2 19.3
Datangpo Fm ZK2115-H19 1,627.40 0.07 3.22 −5.42 −8.91 −31.95 1.6 3.4 5.7 25.4
Mn-carbonate unit WX-32 1,627.90 0.04 −9.55 −8.17 2.8 1.3 18.3 80.3
ZK2115-H18 1,628.40 0.05 4.77 −7.25 −9.32 −32.81 2.1 1.2 18.1 49.4
WX-33 1,628.90 0.05 4.06 2.6 0.6 24.5 63.0
ZK2115-H17 1,629.40 0.07 3.87 −7.05 −7.64 −32.22 1.8 3.0 9.7 28.9
WX-34 1,629.90 0.04 −8.21 −9.55 −32.55 2.6 0.5 22.8 81.3
ZK2115-H16 1,630.40 0.10 2.72 −7.48 −10.41 −32.85 2.0 4.1 0.9 23.2
WX-35 1,630.90 0.04 −8.50 −10.25 −33.11 2.7 0.6 24.0 76.0
ZK2115-H15 1,631.40 0.09 2.04 −33.19 2.9 3.0 0.9 38.8
WX-36 1,631.70 0.12 2.67 −7.41 −9.02 −32.39 1.6 5.5 2.8 14.9
ZK2115-H14 1,632.00 0.03 −9.25 −9.15 −33.47 2.6 0.5 26.1 107.5
ZK2115-H13 1,632.40 0.06 3.78 −8.82 −9.38 −33.21 2.3 2.1 14.2 44.5
ZK2115-H12 1,632.80 0.08 3.69 −5.22 −6.12 −31.82 2.1 3.1 8.5 31.2
ZK2115-H11 1,633.10 0.02 5.26 −8.78 −9.41 −32.62 1.1 0.3 24.5 64.1
ZK2115-H10 1,633.40 0.08 4.95 −8.69 −8.14 −33.16 2.2 0.7 24.9 31.2
ZK2115-H9 1,633.70 0.04 3.29 −9.69 −7.41 −33.09 2.6 1.2 19.9 73.0
ZK2115-H8 1,634.10 0.08 1.53 −32.40 3.1 4.1 0.2 43.0
ZK2115-H7 1,634.60 0.02 4.17 −8.97 −9.72 −33.61 2.5 0.3 26.9 128.6
ZK2115-H6 1,635.10 0.11 2.57 −6.71 −8.52 −32.66 2.2 4.1 7.9 24.6
ZK2115-H5 1,635.40 0.10 2.93 −7.97 −10.36 −32.58 2.2 4.2 2.2 25.6
ZK2115-H4 1,635.70 0.02 −9.41 −4.81 −33.22 1.7 0.8 22.4 78.1
ZK2115-H3 1,636.25 0.03 −10.40 −7.70 −33.31 1.9 0.7 23.1 80.0
ZK2115-H2 1,636.55 0.03 −11.17 −7.46 −33.32 2.3 0.8 21.2 99.7
ZK2115-H1 1,637.15 0.09 1.67 −32.96 2.4 4.2 0.4 30.7

TOC, K2O, and Mn contents of whole rock samples are from Wang et al. (2019b, 2020).

Geochemical profiles of drillcore ZK2115 for the first member of the Datangpo Fm, located in the Gaodi Deposit, Guizhou Province. TOC and Mn contents are collected from Wang et al. (2019b).

 Discussion The nitrogen and carbon isotope evaluation of the post-Sturtian Datangpo Fm

The nitrogen isotope compositions of sedimentary rocks are used to reflect local redox conditions in the water column of ancient oceans and reconstruct biogeochemical N cycling (e.g., Sigman et al., 2009; Quan et al., 2013; Ader et al., 2014, 2016; Stüeken et al., 2016). However, the δ15N can be altered during diagenesis and metamorphism to some extent (Robinson et al., 2012; Ader et al., 2016). The δ15N values can be elevated by 3‰–5‰ under oxic diagenesis (Lehmann et al., 2002; Robinson et al., 2012), but the δ15N values would not alter or only decrease slightly (~1‰) due to anaerobic degradation of organic matter under anoxic conditions (Freudenthal et al., 2001; Lehmann et al., 2002; Möbius et al., 2010; Robinson et al., 2012). During the metamorphism, isotopically light N would preferentially escape, resulting in higher δ15N in residual N reservoirs (Ader et al., 2014). The N geochemical signals in sediments can also be influenced by continental input, but the detrital components in the Datangpo Fm were sourced from flood basalt weathering (Yu et al., 2016), and no significant relationship was found between Al2O3 and δ15N in the Datangpo Fm (Wu et al., 2024); thus, the input of continental N was limited in the first member of the Datangpo Fm.

Nitrogen can be preserved in rocks as two forms, i.e., organic N in organic matter and ammonium (NH4 +) bound with clay minerals. Up to 60% of sedimentary N can be bound with clays as NH4 + within the sediments (Müller, 1977). The positive relationship between TOC and TN indicates that N is sourced from marine primary organic matter (Calvert, 2004), while the weak or no relationship indicates inorganic clay-bound N or reflects terrigenous inputs (Calvert, 2004; Bristow et al., 2009). NH4 + has a similar charge and size to K+, which can substitute for K+ in phyllosilicates (Müller, 1977; Freudenthal et al., 2001) after being released through the degradation of organic matter (Busigny and Bebout, 2013; Stüeken et al., 2016). In this study, TOC and TN show no relationship ( Figure 4A ), but K2O and TN show positive relationships in the Mn-carbonate unit [r = + 0.92, p(α) < 0.001] and the black shale unit [r = + 0.66, p(α) < 0.01] ( Figure 4B ), indicating that the N in sediments was bound with silicate, which were transferred from organic matter.

Cross-plots of TOC-TN (A), K2O-TN (B), C/N-δ15N (C), TN-δ15N (D), TN-C/N (E), and K2O-δ15N (F) in the Mn-carbonate unit (red color) and the overlying black shale unit (blue color) of the Datangpo Fm in the drillcore ZK2115. TOC and K2O contents are collected from Wang et al. (2019b, 2020).

During the burial diagenesis and metamorphism, organic N can be preferentially lost over organic carbon, resulting in higher C/N ratios. The Datangpo Fm did not experience metamorphism; thus, the metamorphic influence on δ15N can be negligible (Tu et al., 2024; Wu et al., 2024). C/N shows no relationship with δ15N in the study units ( Figure 4C ), indicating that the preferential loss of N during burial diagenesis did not alter the δ15N values (Cremonese et al., 2013). However, TN shows negative relationships with δ15N [r = −0.66, p(α) < 0.01] ( Figure 4D ) and C/N [r = −0.87, p(α) < 0.001] ( Figure 4E ) in the Mn-carbonate unit, but no relationships in the black shale unit ( Figures 4D, E ). Furthermore, the K2O and δ15N show a negative relationship in the Mn-carbonate unit [r = −0.80, p(α) < 0.001], but no relationship in the black shale unit ( Figure 4F ). These findings indicated that the N signals were altered by early diagenesis in the Mn-carbonate unit, but the initial signals were preserved in the black shale unit.

The sedimentary carbonates record contemporaneous paleo-ocean chemistry and can be used to reflect ancient ocean information. However, carbonates are susceptible to post-depositional diagenesis, which can overprint primary geochemical signals, such as the concentrations of trace element (Mn, Fe, Ca, and Sr) and isotope compositions (δ13C and δ18O) (e.g., Swart, 2015; Swart and Oehlert, 2018; Reis et al., 2019). Considering that Ca and Sr can be replaced by Fe and Mn from carbonate lattice during diagenesis, the elemental ratios, such as Mn/Sr and Fe/Sr, can be used to identify diagenetic alteration (e.g., Banner and Hanson, 1990; Kaufman and Knoll, 1995; Kouchinsky et al., 2008; Swart, 2015). The sediments in the Mn-carbonate unit of the Datangpo Fm were affected by strong hydrothermal activity, which can provide extra Mn and Fe to the sediments (Wu et al., 2016; Tan et al., 2021; Li et al., 2022); thus, the element ratios cannot be used to reflect diagenetic alteration in this study.

Diagenesis can also decrease the original δ13C and δ18O values in carbonates (e.g., Kaufman and Knoll, 1995; Melezhik et al., 2005; Derry, 2010; Swart, 2015; Reis et al., 2019), and the δ18O values are more sensitive to diagenetic alterations (e.g., Banner and Hanson, 1990; Kaufman et al., 1991; Ray et al., 2003; Swart, 2015). When δ18O > −10‰, it indicates a small effect of diagenesis (Kaufman and Knoll, 1995). Meanwhile, the positive correlation between δ13Ccarb and δ18O values is another sensitive indicator of diagenetic alterations (e.g., Kaufman and Knoll, 1995; Knauth and Kennedy, 2009; Derry, 2010; Bishop et al., 2014; Swart, 2015; Swart and Oehlert, 2018). In recent studies, the correlation between δ13Corg and δ13Ccarb values is also used to evaluate the influence of diagenesis. If sedimentary carbonates are not influenced by meteoric water (Oehlert and Swart, 2014), the covaried δ13Corg and δ13Ccarb values are thought to retain original carbon isotope records (e.g., Knoll et al., 1986; Johnston et al., 2012; Meyer et al., 2013). In this study, the δ18O values of most samples in the Mn-carbonate unit are higher than −10‰, the δ13Ccarb and δ18O values show no relationship ( Figure 5A ), and the δ13Corg and δ13Ccarb values show a strong positive correlation [r = + 0.85, p(α) < 0.001] ( Figure 5B ), implying that the δ13Ccarb values are not altered by diagenesis. Based on the diagenetic indicators, the Mn-carbonate unit recorded original carbon isotope signals and can be used to trace paleo-ocean geochemical information.

Cross-plots of δ13Ccarb-δ18O (A) and δ13Ccarb-δ13Corg (B) in the Mn-carbonate unit of the Datangpo Fm in the drillcore ZK2115.

 Redox conditions of the deep basin and constraints on manganese mineralization in the Cryogenian Nanhua Basin

Nitrogen has multiple valence states (−3 to +5) and is preserved as different types depending on redox conditions (Ader et al., 2014, 2016; Sigman et al., 2009; Canfield et al., 2010; Stüeken et al., 2016). The nitrogen species are complex, including nitrate, nitrite, ammonium, and N2. The transformation between different species occur through different pathways, such as N2 fixation, nitrification, denitrification, and anammox, which are accompanied by different N isotope fractionations (i.e., δ15Nproduct − δ15Nreactant). As atmospheric N2 cannot be directly utilized by most living organisms, N2 fixation by aerobic or anaerobic autotrophs (nitrogen fixers) is the only pathway for atmospheric N2 to enter the marine N cycle. Atmospheric N2 is transferred to organic matter as NH4 + through N2 fixation, and this process generates minor N isotope fractionation (−2‰ to +1‰), except under Fe2+-enriched conditions or in thermophilic cultures where it can reach −4‰ (Zerkle et al., 2008; Stüeken et al., 2016). Bioavailable N in the ocean (e.g., NH4 + and NO3 −) is originally sourced from organic matter. Nitrification, which can transfer NH4 + to NO3 −, occurs under oxic conditions. When NH4 + is partially oxidized, the residual NH4 + is enriched with 15N. Denitrification occurs in anoxic water columns and sediments, and can transfer NO3 − to N2. When NO3 − is completely consumed, the N isotope generates no isotope fractionation. However, when NO3 − is not completely consumed in the water columns, 14N-enriched NO3 − is preferentially reduced, resulting in significant N isotope fractionation (~−20% to −30%; Sigman et al., 2009). The N isotope fractionation during denitrification that occurs under anoxic sediments is negligible, because NO3 − is completely consumed in porewater (Sigman et al., 2009; Cremonese et al., 2013). Anammox occurs under strictly anoxic conditions, and N2 is generated through the reaction of NH4 + and NO2 -. This is another important pathway by which N is lost from the ocean N cycle.

In the Mn-carbonate unit and the black shale unit of the Datangpo Fm, N was bound to silicates, which was sourced from organic matter. N was initially preserved in organic matter as NH4 + and formed through N2 fixation. The δ15N values of organic matter N were low, because of the minor N isotope fractionation during this process and the low δ15N values of atmospheric N2 (0‰). During the sinking of the generated organic matter into the sediments, the oxidation processes almost had no effect on the N-bearing biomass (Wu et al., 2024). When NH4 + was released from organic matter during organic matter mineralization, there was small isotope fractionation owing to its efficiency (Möbius, 2013). If the released NH4 + remains stable under anoxic conditions, N isotope fractionation during non-quantitative NH4 + assimilation can be significant (Δorg-NH4+: up to −27‰) when [NH4 +] is greater than 20 μM, resulting in 15N-depleted organic matter (Pennock et al.,1996; Stüeken et al., 2016), but it decreases strongly as the availability of NH4 +increases, and no fractionation is generated when it is completely consumed. The elevated δ15N values in sediments throughout Earth’s history might be related to intense denitrification under suboxic conditions, compared with the relatively low δ15N values recorded under oxic and anoxic conditions (e.g., Quan et al., 2013), but other studies attributed this to oxic diagenesis (Stüeken et al., 2016). When the released NH4 + was partially oxidized under oxic conditions, oxidation rate was rapid, and 14N was preferential oxidized, resulting in residual NH4 + characterized by higher δ15N values. The nitrification of NH4 + generated the highest δ15N in sediments at ~2.7 Ga (up to +50‰; Thomazo et al., 2011). Considering the changes in TN and δ15N during early diagenesis, the deep water was probably oxic during the precipitation of the Mn-carbonate unit, which can result in a negative relationship between TN and δ15N ( Figure 4D ), whereas the deep water was anoxic during the precipitation of the black shale unit.

In the Mn-carbonate unit of the Datangpo Fm, the Mn contents show a strong negative relationship with TN [r = −0.86, p(α) < 0.001] ( Figure 6A ), but a positive relationship with δ15N [r = +0.85, p(α) < 0.001] ( Figure 6B ), implying that the metallogenesis of the manganese deposits was related to N geochemical signals. When large amounts of Mn-carbonates were reduced from Mn-oxides/oxyhydroxides, abundant organic matter can be degraded, accompanied by enhanced release of NH4 +. However, low contents of N and 15N-enriched NH4 + were transferred to silicate, indicating that 14N-enriched NH4 + was preferentially consumed, which may be related to oxic conditions in the deep basin. Under oxic conditions, significant N isotope fractionation can occur when NH4 + was partially oxidized, resulting in residual NH4 + characterized by relatively higher δ15N values.

Cross-plots of Mn-TN (A), Mn-δ15N (B), TOC-δ13Corg (C), TOC-δ13Ccarb (D), Mn-TOC (E), and Mn-δ13Ccarb (F) in the Mn-carbonate unit (red color) and the overlying black shale unit (blue color) of the Datangpo Fm in the drillcore ZK2115. TOC and Mn contents are collected from Wang et al. (2019b).

The redox conditions in the deep Nanhua Basin are not clear in the basal Datangpo Fm. For example, Fe speciation in the Mn-carbonate unit of the Datangpo Fm recorded oxic intervals in the Yangjiaping section (Li et al., 2012), but anoxic conditions in the Xiushan section (Ma et al., 2019), Gaodi and Xixibao sections (Cheng et al., 2021), Daotuo and Datangpo sections (Wu et al., 2024), and the overlying black shale unit (cf. Wu et al., 2024). Additionally, Corg:P and Ce/Ce* recorded oxic–suboxic conditions in the Mn-carbonate unit and anoxic conditions in the black shale unit (Yu et al., 2016; Xiao et al., 2017; Ai et al., 2021). The findings of this study showed that the Mn-carbonate unit recorded oxic intervals, and the redox variations in the deep Nanhua Basin were related to the episodic ventilation by density flow, which can transfer oxygen to deep water and result in intermittent oxygenation (Yu et al., 2016). Episodic ventilation facilitated the metallogenesis of the manganese deposits in the Nanhua Basin, and the dissolved Mn2+ was first oxidized to Mn-oxides/oxyhydroxides in the oxic deep Nanhua Basin, which were reduced and ultimately preserved as Mn-carbonates in the sediments (Yu et al., 2016, 2017; Wu et al., 2016; Xiao et al., 2017).

 Anomalous δ<sup>13</sup>C<sub>carb</sub> excursions in the post-Sturtian Nanhua Basin, South China Carbon isotope evolution of organic matter after the Sturtian Glaciation

Based on the Snowball Earth hypothesis (Kirschvink, 1992; Hoffman et al., 1998; Hoffman and Schrag, 2002), the ice sheet prevailed on Earth during Neoproterozoic global glaciations, and even reached the equator. However, the ecosystem did not completely collapse during the extreme icehouse climate. For example, the evidence of organic molecules and biomarkers indicates that photosynthesis never ceased during the Sturtian Glaciation, even though the rate was low (Olcott et al., 2005; Wang et al., 2008; Riedman et al., 2014). The organic matter generated through photosynthesis was preserved in glacial sediments, which were characterized by low TOC contents (mean 0.12%; McKirdy et al., 2001; Olcott et al., 2005; Pei et al., 2020).

After the Sturtian Glaciation, the ice sheet melted, accompanied by a transition from icehouse climate to greenhouse climate (Hoffman et al., 1998; Yonkee et al., 2014; Scheller et al., 2018), and the chemical weathering intensity was enhanced, leading to the transfer of large amounts of nutrients into the ocean (e.g., Rieu et al., 2007; Zhu et al., 2019; Ai et al., 2020a; Wang et al., 2020; Wei et al., 2020; Li et al., 2022). At the end of the Sturtian Glaciation, microbes began to flourish (e.g., Zhu et al., 2019; Ai et al., 2020b). The planktonic biotas were widespread and abundant after the glaciation (Riedman et al., 2014). Moreover, the rise of algae (including cyanobacteria) with great diversities contributed to the organic matter inputs in the post-Sturtian sediments (Brocks et al., 2017; Zhu et al., 2019; Ai et al., 2020b). In the Nanhua Basin, the post-Sturtian Datangpo Fm sediments were strongly affected by hydrothermal activity (Wu et al., 2016; Yu et al., 2016; Tan et al., 2021; Li et al., 2022), which can also provide essential nutrients for life in the ocean, promoting microbial breeding and increasing the rate of photosynthesis (Tribovillard et al., 2006; Dick et al., 2013).

In this study, the Mn-carbonate unit and the black shale unit of the Datangpo Fm are characterized by high TOC contents (mean 2.2% and 1.8%, respectively; Wang et al., 2019b) ( Figure 3 ), which are consistent with previous studies in this basin ( Figure 7 ; e.g., Wei et al., 2016; Zhu et al., 2019, 2022; Ai et al., 2020a, 2021; Tan et al., 2021; Li et al., 2022; Zhao et al., 2022). The high TOC contents were also recorded in the coeval clastic sedimentary sequences, such as the Twitya Fm in Canada (Sperling et al., 2016), the Arena Fm in East Greenland (Scheller et al., 2018), the MacDonaldryggen Member of the Elbobreen Fm in Svalbard (Kunzmann et al., 2015), and the Tapley Hill Fm and Aralka Fm in Australia (McKirdy et al., 2001; Bowyer et al., 2023). The TOC contents show a decreasing trend from the Mn-carbonate unit and black shale unit to the overlying gray shales (only discovered in limited areas) and the second member of the Datangpo Fm (mean 0.25% and 0.12%, respectively; Li et al., 2012; Peng et al., 2019; Zhu et al., 2019, 2022; Shen et al., 2022). This finding may be related to the elevated oxygenated environment and rapid deposition rates, which were not conducive to the preservation of organic matter (Zhu et al., 2019). Whether the organic matter preserved in the sediments was derived from primary productivity through photosynthesis needs to be further studied. The detrital materials of the first member of the Datangpo Fm were sourced from weathering of continental flood basalts (Yu et al., 2016; Ai et al., 2020a), and the amount of recycled organic matter input from continents was small; thus, this kind of organic matter in the Datangpo Fm can be ignored (Burdige, 2007; Peng et al., 2019). Thermal maturation during diagenetic or metamorphic processes preferentially removes the light isotopic composition for organic carbon isotopes, resulting in negative correlations between the TOC and δ13Corg values (Clayton, 1991; Hayes et al., 1999), but the TOC and δ13Corg values in the study sections show no relationship ( Figure 6C ), indicating that the δ13Corg values were not altered by diagenetic or metamorphic alterations. Additionally, the microbial sulfate reduction process played a significant role during the organic matter degradation, but the seawater sulfate concentration in Neoproterozoic was extremely low (Hurtgen et al., 2002; Zhao et al., 2022), implying that organic matter consumption by microbial sulfate reduction was extremely low. The above findings showed that the organic matter preserved in the Datangpo Fm was mainly the product of photosynthesis after the glaciation and recorded the original carbon isotope signals.

Mn, TOC, and δ13C profiles for first member of the Datangpo Fm of Lijiawan area (A; Li et al., 2022), Datangpo area (B, C; Zhou et al., 2007; Tan et al., 2021), Gaodi area (D; Pei et al., 2020), and Yanglizhang area (E; Zhu et al., 2019) in Guizhou Province and Gaodongyuan area in Chongqing City (F; Zhu et al., 2019). TSA, Tiesi’ao Fm.

The carbon isotope compositions of organic matter show a gradually increasing trend from the Mn-carbonate unit (mean −32.46‰) to the overlying black shale unit (mean −31.20‰) ( Figures 3 , 7 ), and this shift can also be observed in other sections across the Nanhua Basin (e.g., Wei et al., 2016; Ai et al., 2020a, 2021; Pei et al., 2020; Tan et al., 2021; Li et al., 2022). The high-resolution δ13Corg values also show an increasing tendency in the complete Datangpo Fm between the Sturtian and Marinoan glaciations (Peng et al., 2019; Zhu et al., 2022; Bowyer et al., 2023), which was consistent with the MacDonaldryggen Member of the Elbobreen Fm in Svalbard (ca. −34.0‰ to −30.4‰, Halverson, 2011; Ader et al., 2014) and the Arena Fm in East Greenland (−33.7‰ to −30.7‰, Scheller et al., 2018). The increasing δ13Corg values in the post-glacial sediments may be related to the burial of large amounts of organic matter. During photosynthesis, the lighter 12C was preferentially utilized and incorporated into organic matter, resulting in low δ13C values of organic matter. With the increasing burial of organic matter into post-glacial sediments, large amounts of 12C were fixed in the sediments, resulting in higher carbon isotope compositions of organic matter generated in later stages. Therefore, the long-term organic carbon isotope evolution in the post-Sturtian interval was related to the burial of organic matter generated through photosynthesis.

 The negative δ<sup>13</sup>C<sub>carb</sub> excursions in the manganese deposits of the Nanhua Basin

The Mn-carbonate unit of the Datangpo Fm is characterized by negative carbon isotope excursions, ranging from −11.17‰ to −5.22‰ with a mean of −8.30‰ ( Figure 3 ), similar to the carbon isotope compositions of coeval manganese deposits in the Nanhua Basin, such as Datangpo, Xiushan, Gucheng, and Xiangtan manganese deposits ( Figure 7 ; e.g., Li et al., 1999; Zhou et al., 2007; Chen et al., 2008; Wu et al., 2016; Qu et al., 2018; Zhu et al., 2019; Pei et al., 2020; Tan et al., 2021; Dong et al., 2023). The δ13Ccarb values of the Mn-carbonate unit are lower than those of the overlying black shale unit in South China (−6.76‰ to −5.15‰, mean −5.94‰; Zhu et al., 2019) ( Figure 7F ) and coeval marine clastic sediments globally, such as the Arena Fm shales in East Greenland (−7.88‰ to +1.42‰, mean −3.39‰, n = 18; Scheller et al., 2018) and the Tindelpina Shale Member of the Tapley Hill Fm in South Australia (−6.7‰ to +1.5‰, mean −3.59‰, n = 39; McKirdy et al., 2001; Giddings and Wallace, 2009). However, the δ13Ccarb values of the basal Datangpo Fm are lower than the carbon isotope compositions of the mantle (−5‰; Kump and Arthur, 1999); thus, the influence of the mantle on the negative carbon isotope excursions can be excluded. Many studies suggested that this phenomenon was related to organic matter degradation, which can provide 13C-depleted carbon (Li et al., 1999; Chen et al., 2008; Wu et al., 2016; Qu et al., 2018; Zhu et al., 2019). The TOC and δ13Ccarb show no relationship (Figure 6D), indicating that the inorganic carbon isotope compositions of the Mn-carbonates were not influenced by the TOC contents. Meanwhile, the Mn contents show no relationship with TOC ( Figure 6E ), but a negative relationship with δ13Ccarb [r = −0.66, p(α) < 0.01] ( Figure 6F ), implying that the organic matter was sufficient for the Mn reduction and that the δ13Ccarb values were influenced by Mn-carbonate formation. The elevated Mn-carbonate formation indicated enhanced organic matter mineralization, resulting in more 12C-enriched C being transferred to CO3 2− and ultimately preserved in Mn-carbonates, which were characterized by lower δ13Ccarb values. Therefore, the negative carbon isotope excursions in the post-Sturtian Nanhua Basin were related to the metallogenic process of the manganese deposits, similar to the Ediacaran manganese deposits in the northern margin of the Yangtze Block (Zhang et al., 2024a, 2024b). These lines of evidence also suggested that the Mn-carbonates were mainly precipitated with the precursor of Mn-oxides/oxyhydroxides (Yu et al., 2016, 2017; Wu et al., 2016; Xiao et al., 2017). However, a previous study suggested that part of Mn-carbonates can precipitate directly from anoxic water columns, which are characterized by small grains (<2 μm) and core–shell structures (i.e., a minor Ca-carbonate core enclosed by a Mn-carbonate shell) (Ai et al., 2023). This process of Mn-carbonate formation can occur when the deep basin was episodic anoxic, but it is not the major metallogenic process. Furthermore, only small amounts of Mn-carbonates can be formed through this process.

 N–C cycling in the post-Sturtian Nanhua Basin, South China

Based on this study, we propose a new nitrogen and carbon cycling model for the post-Sturtian Nanhua Basin. During the Sturtian Glaciation, photosynthesis rates were relatively weak during extreme icehouse climate, and the recorded OM contents in glacial sediments were low (mean 0.12%; McKirdy et al., 2001; Olcott et al., 2005; Pei et al., 2020). After the Sturtian Glaciation, the ice sheet melted accompanied by the transition to greenhouse climate. The ecosystem recovered, photosynthesis rates increased dramatically, and 12C was preferentially utilized and incorporated into the organic matter during this process (Knauth and Kennedy, 2009). Large amounts of organic matter generated by photosynthesis were preserved in the Mn-carbonate unit of the Datangpo Fm, which was characterized by high TOC contents (mean 2.2%) with a mean δ13Corg of −32.84‰ ( Figure 8A ). During the formation of organic matter, atmospheric N2 was fixed in organic matter as NH4 +. The organic matter (including Norg) then sank into the sediments. During the postglacial interval, episodic ventilation in the deep Nanhua Basin transferred large amounts of oxygen into the deep basin (Feng et al., 2010; Li et al., 2012; Yu et al., 2016; Dong et al., 2023), which led to intermittent oxic conditions in the deep Nanhua Basin. Hydrothermally sourced Mn2+ was oxidized to Mn-oxides/oxyhydroxides and then reduced to Mn-carbonates after being co-buried with organic matter in the sediments (Yu et al., 2016, 2017; Wu et al., 2016; Xiao et al., 2017). During this process, organic matter acted as an electron acceptor and facilitated the reduction of Mn-oxides/oxyhydroxides. During early diagenesis, Norg was preferentially released over Corg. Moreover, Norg was released as NH4 + from organic matter, part of which was oxidized to NO3 − in the oxic deep basin, and significant N isotope fractionations were generated during this process. This residual NH4 + was bound with silicates and characterized by elevated δ15N values (mean +3.36‰). During organic matter mineralization driven by Mn-carbonate formation, 13C-depleted C led to negative δ13Ccarb excursions (mean −8.30‰).

Nitrogen and carbon cycling model in the Mn-carbonate unit (A) and the black shale unit (B) of the Datangpo Fm after the Sturtian Glaciation.

During the deposition of the black shale unit of the Datangpo Fm, the photosynthesis rates were still high, and the sediments were also characterized by high TOC contents (mean 1.8%) ( Figure 8B ). With the burial of 13C-depleted organic matter after the Sturtian Glaciation, the latterly formed organic matter was characterized by higher carbon isotope compositions (mean −31.20‰), which caused the δ13Corg values in the black shale unit to be higher than the Mn-carbonate unit and show an increasing trend during the postglacial interval ( Figure 3 ). During this period, the deep water was anoxic and covered by oxic surface water. After the OM (including Norg) sank, NH4 + was released from the organic matter, part of which diffused into anoxic deep water without N isotope fractionation. The residual NH4 + was bound to silicate, which recorded the original δ15N signals (mean +0.89‰). Moreover, the seawater DIC reservoir in the black shale unit inherited the carbon isotope compositions of the Mn-carbonate unit, but the organic matter degradation facilitated by Mn-carbonate formation ceased; thus, the 13C-depleted carbon input was lacking. Therefore, the δ13Ccarb values in sediments showed negative δ13Ccarb excursions (mean −5.81‰; Zhu et al., 2019; Pei et al., 2020) but were greater than the underlying Mn-carbonate unit (mean −8.30‰).

 Conclusions

The Nanhua Basin of South China recorded the complete Cryogenian stratigraphic sequence from the Sturtian to the Marinoan glaciations, and the manganese deposits precipitated in the interglacial Datangpo Fm. The main findings of this study are as follows:

After the Sturtian Glaciation, the Mn-carbonate unit is characterized by relatively high δ15N values (mean +3.66‰), implying the oxic conditions in the Mn-carbonate unit. The oxic deep basin facilitated the Mn2+ oxidation to Mn-oxides/oxyhydroxides, which were ultimately reduced and preserved as Mn-carbonates in the sediments. Therefore, the metallogenic process of the manganese deposits was mainly constrained by redox variations, which experienced two stages. The overlying black shale unit is characterized by relatively low δ15N values (mean +0.89‰), indicating the anoxic conditions during this period.

During the reduction of Mn-oxides/oxyhydroxides, organic matter was mineralized, resulting in 13C-depleted CO3 2− being formed and preserved in Mn-carbonates. The Mn-carbonate unit recorded the negative δ13Ccarb excursions (mean −8.30‰), which were caused by the Mn-carbonate formation. Carbon cycling in the deep Nanhua Basin was strongly affected by the metallogenesis of the Cryogenian manganese deposits.

The nitrogen and carbon cycling processes in the post-Sturtian Nanhua Basin were influenced by redox variations, and the N–C cycling model in the Cryogenian Nanhua Basin was reconstructed. This model can also provide new insights for the biogeochemical cycling in other ocean systems.

 Data availability statement

The original contributions presented in the study are included in the article/supplementary material. Further inquiries can be directed to the corresponding author.

 Author contributions

PW: Writing – original draft, Writing – review & editing. JW: Writing – original draft. YD: Writing – review & editing. WY: Writing – review & editing. QZ: Writing – review & editing. LT:Writing – review & editing. LY: Writing – review & editing. WP: Writing – review & editing. WW: Writing – review & editing. YQ: Writing – review & editing. ZM: Writing – review & editing.

 Funding

The author(s) declare financial support was received for the research, authorship, and/or publication of this article. This work was supported by the National Natural Science Foundation of China (No. 42202111), the Open Research Program of State Key Laboratory of Biogeology and Environmental Geology, China University of Geosciences (Wuhan) (No. GBL22107), the Postdoctoral Foundation and Key Scientific Research Project of Henan Province, China (No. HN2022027 and No. 24A170019), and the Open Fund of Engineering Technology Innovation Center of Mineral Resources Explorations in Bedrock Zones, Ministry of Natural Resources (No. MREBZ-2023-OF01).

 Acknowledgments

We thank the editors and reviewers for their constructive comments. We are grateful to the officers of China University of Geosciences (Wuhan) for the lab work.

 Conflict of interest

The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.

 Publisher’s note

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