Thank you for visiting nature.com. You are using a browser version with limited support for CSS. To obtain the best experience, we recommend you use a more up to date browser (or turn off compatibility mode in Internet Explorer). In the meantime, to ensure continued support, we are displaying the site without styles and JavaScript.

# Around one third of current Arctic Ocean primary production sustained by rivers and coastal erosion

## Abstract

Net primary production (NPP) is the foundation of the oceans’ ecosystems and the fisheries they support. In the Arctic Ocean, NPP is controlled by a complex interplay of light and nutrients supplied by upwelling as well as lateral inflows from adjacent oceans and land. But so far, the role of the input from land by rivers and coastal erosion has not been given much attention. Here, by upscaling observations from the six largest rivers and using measured coastal erosion rates, we construct a pan-Arctic, spatio-temporally resolved estimate of the land input of carbon and nutrients to the Arctic Ocean. Using an ocean-biogeochemical model, we estimate that this input fuels 28–51% of the current annual Arctic Ocean NPP. This strong enhancement of NPP is a consequence of efficient recycling of the land-derived nutrients on the vast Arctic shelves. Our results thus suggest that nutrient input from the land is a key process that will affect the future evolution of Arctic Ocean NPP.

## Introduction

Primary production in the Arctic Ocean by unicellular phytoplankton forms the basis of a unique ecosystem that supports a rich wildlife with some of Earth’s most iconic top predators, such as polar bears or walrus1. The nutrients supporting this marine primary production, and especially the limiting nutrient nitrogen2,3, are believed to stem largely from lateral input from the adjacent oceans and from upwelling and mixing from below4. Not well known is the role of the nutrients supplied to the Arctic Ocean from land via rivers and through the erosion of coastal soils. Understanding the role of these terrigenous nutrients on Arctic Ocean NPP is of paramount importance, especially as the Arctic Ocean and its catchment are one of the world’s fastest-changing regions, mostly due to anthropogenic climate change5.

It has been estimated that Arctic Ocean NPP increased by 57% between 1998 and 2018 due to warming, sea-ice reduction, and changes in ocean circulation6,7. Model simulations have suggested that this increase will continue in the 21st century8 and has the potential to significantly enhance fisheries catch in the Arctic Ocean9. However, the models used for these projections differ strongly in their simulated present-day10 and future Arctic Ocean NPP8 due to the complex interplay of nutrient and light limitation of phytoplankton production. Differences between these models, as well as observed changes in NPP6,7,11 have mainly been related to the specific physical conditions of the Arctic Ocean, such as sea-ice extent and ocean circulation. However, recent studies have suggested that terrigenous nutrient inputs from rivers and coastal erosion might be another key control of Arctic Ocean NPP12,13,14, a process that has often been neglected in observational studies6,7,11 and models8,10.

Neglecting the role of terrigenous nutrients is particularly problematic in the Arctic Ocean, as their impact on marine NPP is presumably large compared to other ocean regions due to the Arctic Ocean’s unique geographical setting. The Arctic Ocean is the only ocean that has a watershed area that is larger than its own area. It receives around 11% of global river discharge although it holds only 1% of the global ocean volume15. In addition, the Arctic coastline is eroding fast due to thawing permafrost, providing another important source of terrigenous nutrients13,16.

Despite the potential importance of terrigenous nutrient inputs for Arctic Ocean NPP, the magnitude of these fluxes12,16,17 and their net impact on Arctic Ocean NPP are not well known13,18,19,20. Measurements of the riverine nutrient fluxes were taken frequently at the six largest Arctic rivers (Mackenzie, Yukon, Kolyma, Lena, Ob, Yenisei)12,21,22, and were periodically recorded in several smaller river systems23,24,25,26, but few time series of observations were collected elsewhere. Thus, to estimate the total riverine fluxes of carbon and nutrients into the Arctic Ocean, the fluxes from the six largest rivers were extrapolated to the entire Arctic catchment18,20,21,27. Riverine nutrient inputs determined from previously published pan-Arctic organic carbon fluxes were used to estimate riverine-driven NPP to vary between 418 and 10%19,20 of total Arctic NPP. In contrast to riverine nutrient fluxes, no estimates of nutrient fluxes from coastal erosion and of their impact on Arctic NPP exist yet, mainly because of the limited number of observations of nutrient content in the eroded soils28,29.

Here we provide (1) a gridded estimate of the seasonally varying river input of dissolved nutrients and carbon, (2) a gridded estimate of the seasonally varying input of nutrients and carbon from coastal erosion and (3) a quantitative assessment of the importance of these two sources of nutrients for Arctic Ocean NPP. To do so, we derived a monthly, spatially resolved, observation-based forcing set for riverine dissolved terrigenous carbon and nutrient inputs to the coastline north of 60°N. These riverine fluxes are based on observed monthly fluxes from the six largest Arctic rivers12,21, which were extrapolated to unmonitored river basins using a spatially explicit prediction based on watershed characteristics (see Methods). For coastal erosion, total (particulate + dissolved) terrigenous carbon and nutrient inputs were calculated as the product of spatially resolved erosion rates30 and estimates of total carbon and nutrient content in coastal soils28,29,30,31. The riverine and coastal erosion fluxes of nutrients and carbon were then used to force the global ocean-biogeochemical model NEMO-PISCES32 at high-resolution (~14 km in the Arctic Ocean) over the period 1990–2010 (Baseline simulation). The version of NEMO-PISCES used here does not allow us to add organic matter fluxes with carbon-to-nitrogen (C:N) and carbon-to-phosphorus ratios that differ from the stoichiometric marine ratios in the model. Therefore, riverine and coastal erosion fluxes were added in their inorganic form assuming immediate remineralisation of all organic matter at the land-ocean interface (see Methods). We also do not consider the effect of terrigenous particulate matter emanating from the rivers or coastal erosion on turbidity of the waters, and hence the light availability for phytoplankton growth. We later assess the uncertainty and potential bias related to these assumptions and their effect on simulated Arctic Ocean NPP.

In addition to the baseline simulation, we also conducted a simulation without any terrigenous input (Referred to as NoTerr) north of 60°N and one where only the river input was considered (NoCoast). The differences between these three simulations permit us then to quantify the impact of the various forms of terrigenous input. Throughout the rest of the manuscript, we focus on nitrogen given its role as the limiting nutrient for NPP in the Arctic Ocean2,3 (Supplementary Fig. 1).

With these simulations, we estimate that terrigenous nutrients fuel 28–51% of the current annual Arctic Ocean NPP. Our results thus suggest that nutrient input from the land is a key process for Arctic Ocean NPP and its future evolution.

## Results and discussion

### Nitrogen input from rivers

We estimate that rivers currently deliver 1.0 (0.9–1.1) Tg N yr−1 of dissolved nitrogen (inorganic 32% and organic 68%) to the Arctic Ocean, which is limited here by the Fram Strait, the Barents Sea Opening, the Bering Strait, and the Baffin Bay (Table 1; Supplementary Fig. 2). Sixty percent of the dissolved nitrogen that enters the Arctic Ocean by rivers is provided by only five rivers (Mackenzie, Pechora, Ob, Yenisei, Lena) (Fig. 1), and with four of them located in the Russian Arctic, this region dominates the input. The seasonality of the dissolved nitrogen input is strong. During winter, riverine delivery keeps a baseflow of 0.03 Tg N mon−1 (Fig. 2) before increasing during spring freshet to a peak in June (0.33 Tg N mon−1) and then decreasing back to winter baseflow12. Rivers also deliver particulate organic nitrogen, amounting to around 0.7 Tg N yr−122. However, 85–95% of this particulate nitrogen is believed to settle in the river delta33. Given the likely limited impact and the still high uncertainties associated to the biogeochemical cycling of particulate matter across the river‐estuary continuum22, we did not include any riverine input of particulate organic matter in our simulations, but later discuss this additional input and its potential role for Arctic Ocean NPP.

Our dissolved riverine nitrogen fluxes to the Arctic Ocean are in agreement with previous estimates that extrapolated the nutrient fluxes of the six largest Arctic rivers by applying the average yield to unmonitored watersheds12. The agreement is expected as both estimates rely on the same observed flux data and corroborates the use of average yield to upscale fluxes to the pan-Arctic scale. Note, however, that an average yield would probably not reproduce the spatial heterogeneity of nutrient input along the Arctic coastline as it is achieved in our estimate (Fig. 1).

### Nitrogen input from coastal erosion

For coastal erosion, we estimate a delivery of 1.6 (1.0–2.5) Tg N yr−1 of total nitrogen to the Arctic Ocean (Table 1). As opposed to rivers, this nitrogen input occurs almost entirely in particulate organic form34. The spatial distribution of nitrogen input from coastal erosion is more homogeneous, with highest rates along the Eurasian coastline (Fig. 1). Fluxes from coastal erosion peak later in the year (Fig. 2), i.e. they are strongest in August and September (0.45 Tg N mon−1), when sea ice reaches its minimum and coastlines are exposed to wind and waves, and negligible in winter35.

No previous pan-Arctic nitrogen fluxes from coastal erosion exist yet to compare our estimates against. However, we can compare our coastal erosion carbon fluxes, from which the nitrogen fluxes are derived via a fixed C:N ratio, to previous estimates17. These previous pan-Arctic carbon flux estimates from coastal erosion vary from 4.9 to 14.0 Tg C yr−1 with the most recent study being at the high end16. The here presented estimate of 15.4 (9.2–24.2) Tg C yr−1 agrees with the previous estimates within the uncertainties (Table 1) and is 10% above the most recent study. Regionally, our estimates of coastal-erosion-derived carbon flux along the Eurasian coast (12.6 Tg C yr−1) agree with earlier studies (4.0–12.8 Tg C yr−1)17, but are 1.8 Tg C yr−1 (230%) above the earlier estimate in the Beaufort Sea36. The close agreement to the most recent study16 corroborates our estimate of the nitrogen flux from coastal erosion, which, nevertheless, remains highly uncertain (Fig. 2, methods) due to the large uncertainty in the nitrogen content of coastal soils28,29, but also because of a potentially large contribution of nitrogen fluxes from subsea coastal erosion16 that is not accounted for in our Baseline run.

### Net primary production driven by terrigenous nitrogen

The average annual NPP simulated from 2005 to 2010 in the Baseline simulation (including terrigenous nitrogen) is 380 Tg C yr–1 for the Arctic Ocean as defined in this study (Supplementary Fig. 2). When integrated over the larger area north of the Arctic circle, our simulated marine NPP (551 Tg C yr−1) is not significantly different from the remote-sensing-based NPP estimate of 540 ± 25 Tg C yr−1 for the same years6 (Table 2; Fig. 3a, c). Moreover, simulated NPP agrees within uncertainties with the remote-sensing-based estimate within each regional sea except for the Barents Sea, where the simulated value is 23% lower than the remote-sensing-based estimate, and the Chukchi Sea and the ﻿Canadian Arctic Archipelago (CAA), where it is 68% and 59% higher, respectively. These three regions are strongly influenced by inflowing waters from the adjacent oceans. We thus consider this mismatch in NPP to stem from a likely bias in the simulated water inflow, and thus nutrient input, from these oceans37. This is further corroborated by these regions not being strongly affected by the terrigenous nutrient input (Table 2; Fig. 3d).

Without terrigenous nitrogen input (NoTerr), the simulated Arctic Ocean NPP is 138 Tg C yr−1 (36%) lower than in the Baseline simulation where this input is considered (Table 2; Fig. 3b). Both coastal erosion and rivers are important nitrogen sources. By comparing the simulation, wherein only the riverine nutrient input is considered (NoCoast), with the baseline and the NoTerr simulations, we find that coastal erosion sustains around 21% (79 Tg C yr–1) of the Arctic Ocean NPP, while rivers sustain around 15% (58 Tg C yr–1).

The relative amount of NPP sustained by terrigenous nutrients is largest on the Siberian shelves: Kara Sea (59%), Laptev Sea (80%) and East-Siberian Sea (57%) (Table 2, Fig. 3b). Leaving out terrigenous input pushes the simulated NPP on the Siberian shelves well below the range of the remote-sensing-based estimates. Furthermore, these shelf seas receive almost no nutrients from adjacent seas, as nitrogen inflow from the Pacific Ocean is diverted to the Central Arctic by the Transpolar Drift before reaching the Laptev Sea38 and the nitrogen input from the Atlantic Ocean is already consumed in the Barents Sea before reaching the Kara Sea39. Conversely, the regional seas that receive considerable lateral nitrogen input from the adjacent oceans (Barents, East-Siberian, Chukchi, and Beaufort Seas) exhibit a relatively small, but still visible impact on NPP from terrigenous nitrogen. Temporally, the impact of terrigenous nutrients increases steadily over the summer from 22% in May to 47% in September (Fig. 2).

### Recycling rate of terrigenous nutrients

The relatively large contribution of terrigenous nitrogen to Arctic Ocean NPP requires a very efficient recycling of the added nitrogen. Assuming a C:N ratio of 122:16, and assuming that every mol of N is used only once by phytoplankton before it is exported, the total annual input of terrigenous nitrogen of 2.6 Tg N yr−1 would only support a rise in NPP of 17.0 Tg C yr−1, eight times less than the total simulated enhancement in NPP. The much higher stimulation of NPP means that, on average, one mol of terrigenous nitrogen is recycled about seven times before it is exported to the abyss, buried in sediments, or exported laterally to the Pacific or Atlantic Ocean.

This efficient recycling occurs via the remineralisation of marine organic matter in the water column or sediments or via ingestion and excretion by zooplankton. In our simulation, only a small fraction of the marine organic matter produced by the terrigenous nutrients is buried in Arctic sediments (3%) or accumulates as marine dissolved organic matter (3%) and is eventually exported to the adjacent oceans. Instead, most of the organic matter produced by terrigenous nutrients is remineralised, mainly in the sediments (52%) and to a lesser extent within the water column (26%), and recycled via excretion of inorganic nutrients by zooplankton (17%) (Supplementary Fig. 3). Vertically, 88% of the total (water column and sediment) remineralisation occurs at shallow depths (less than 55 m below ocean surface), where around 25% of the Arctic Ocean floor is located (Supplementary Fig. 4).

Benthic processes thus largely contribute to organic matter remineralisation and inorganic nitrogen cycling. Accordingly, the regions with strong NPP and remineralisation are located in very shallow waters where benthic-pelagic coupling is tight (Fig. 3, Supplementary Figs. 2 and 5). Due to the shallow water depth, the cycle of production and remineralisation of organic matter is not dependent on upwelling, as a large fraction of the nutrients is remineralised within the mixed layer. Therefore, we suggest that the large fraction of shallow waters with the associated ﻿extensive organic matter remineralisation in sediments of the Arctic shelves support these high pan-Arctic nutrient recycling rates (~7) and thus the relatively large importance of terrigenous nutrients for the Arctic Ocean NPP in this study. Recycling rates from polynyas in the CAA (0.5–3.2)40,41,42 are thus not representative for the Arctic Ocean. Hence, their application to estimate pan-Arctic riverine-driven NPP18 solely from riverine nitrogen input results in an underestimation of pan-Arctic riverine-driven NPP.

### Considering uncertainties

The results presented here are subject to many uncertainties, in particular associated with missing processes at the land-ocean interface, with the unconstrained reactivity of terrigenous organic matter, with unrepresented terrigenous sources of nitrogen, and with the lack of consideration of the role of terrigenous particulate matter on ocean turbidity. In the following sections, these uncertainties and their potential impact on the amount of nitrogen inputs from land and Arctic NPP are discussed and quantified when possible. This permits us to reassess our model-based estimates of the fraction of the NPP driven by terrigenous sources of nitrogen.

Riverine carbon and nitrogen fluxes are often measured several tens of kilometres upstream from the river mouth12,18 and thus before the transit through the often complex and biologically active river deltas. In the Arctic, deltas are generally smaller in size than in temperate regions and therefore probably less important for the fate of the riverine matter fluxes, with the exception of the Lena and Mackenzie deltas43. In the Mackenzie delta, the concentration of dissolved inorganic nitrogen was found to decrease by 4% across the delta, while that of organic nitrogen increased by 22%, yielding an overall increase in the nitrogen flux43. Thus, the alteration of the nutrient fluxes across a river delta is clearly relevant, but likely remains a local effect. Furthermore, we consider our lack of consideration of the impact of the terrigenous particulate matter on turbidity to have only a minimal impact on our results and conclusions. First, turbidity from particles is globally44 and in the Arctic Ocean45,46 mostly confined to the very nearshore zone and temporally to the spring breakup, as particulate matter from coastal erosion and rivers settles close to its origin33,47. Given the large spatial extent of the Arctic shelves, particles thus only affect a minor part of these shelf seas. Second, while the particles settle quickly out of the euphotic zone, the nutrients remain, unleashing their impact downstream of the river mouth with some delay. Thus, while the consideration of the input of terrigenous particles would result in a spatial and temporal delay of the NPP’s response to an input of terrigenous nutrients, we do not expect any fundamental change in the magnitude of the response. Lacking quantitative information on nutrient dynamics in the river delta and on turbidity in the nearshore zone, we do not apply any pan-Arctic adjustment for both effects, following assumptions made in previous studies12,18,19,20,21.

Our assumption of instantaneous remineralisation of organic nutrients into their inorganic form when delivered to the ocean by Arctic rivers and coastal erosion (see Methods) clearly leads to an overestimation of the amount of nutrients available to fuel primary production. Based on observed remineralisation rates of organic matter48,49,50,51,52 and Arctic Ocean water residence times of freshwater (3.5 ± 2.0 years on Siberian shelves53, 11 years in the Canada Basin54), we estimate that only 60 (20–80)% of riverine dissolved organic nitrogen and 80 (70–90)% of organic nitrogen derived from coastal erosion (see Methods) would be remineralised rapidly enough to fuel Arctic Ocean NPP. Accounting for this “reaction-limited” effect would decrease the input of nitrogen that is available to fuel marine NPP from 1.0 (0.9–1.1) Tg N yr−1 to 0.7 (0.5–0.9) Tg N yr−1 for riverine fluxes and from 1.6 (1.0–2.5) Tg N yr−1 to 1.4 (0.7–2.3) Tg N yr−1 for coastal erosion fluxes.

So far, we have not yet accounted for the input of riverine particulate nitrogen nor nitrogen inputs linked to eroding subsea permafrost. Riverine particulate organic nitrogen input to the Arctic Ocean was previously estimated to be around 0.7 Tg N yr−122. However, only around 5–15% of this input leaves the river delta33 and may contribute to primary production outside the delta. For subsea erosion, the input of organic carbon into the Laptev Sea and the East-Siberian Sea has been estimated at 11 (7–15) Tg C yr−116. Using the same C:N stoichiometric ratio as for Siberian soils and assuming a labile fraction of 70–90% (as for coastal-erosion-derived organic matter) yields a subsea erosion input of organic nitrogen of 1.0 (0.5–1.5) Tg N yr−1. Accounting for these two additional terrigenous sources of nitrogen and for the estimated reactivity of organic matter discussed above would yield a nitrogen input that is available to fuel primary production in the Arctic Ocean from rivers of 0.8 (0.6–1.0) Tg N yr−1 (−20% compared to prescribed nitrogen input) and from coastal erosion of 2.4 (1.2–3.8) Tg N yr−1 (+50%).

### Adjusting the estimate of NPP driven by terrigenous nutrients

These adjustments in the nutrient delivery ask for a revision of our model-derived estimate of terrestrial-driven Arctic Ocean NPP. In order to determine how much NPP will need to be adjusted, we assume that NPP scales linearly with the amount of bioavailable nitrogen supplied by rivers and/or coastal erosion. This linear scaling is corroborated by our three biogeochemical simulations (Baseline, NoCoast, NoTerr), highlighting the N-limited nature of total Arctic Ocean NPP. Using this simple scaling, we adjust the original model-based NPP to 96–255 Tg N yr−1, which corresponds to 28–51% of the total Arctic Ocean productivity (Fig. 4). Rivers would thus account for 32–53 Tg N yr−1 or 9–11% of total Arctic Ocean NPP, while coastal erosion would account for 64–202 Tg N yr−1 or 19–41%. The value at 51% results from a combination of a high nitrogen input and high reactivity and we consider this a likely upper-bound estimate. Such combination would indeed imply low burial efficiency for terrestrial-derived organic matter while several local studies have identified burial as a significant, yet quantitatively uncertain pathway for terrestrial POM in nearshore coastal settings29,47,55,56. However, even if we assumed the lowest possible reactivity of organic material and the lowest range of nitrogen input, the terrigenous driven NPP would still contribute at least 28% of Arctic Ocean NPP (Fig. 4). This is indeed a likely lower-bound estimate, since our simulations showed that terrigenous nitrogen is essential to support a NPP that resembles the remote-sensing-based estimates (Figs. 3 and 4).

### Comparison to previous Arctic Ocean NPP studies

Our assessment suggests a much more prominent imprint of terrestrial inputs compared to previous studies that have estimated the impact of riverine nitrogen on Arctic Ocean NPP. The first study by Tank et al.18 used fixed recycling rates and estimated that riverine nitrogen sustains 1–4% of Arctic Ocean NPP. Two studies by Le Fouest et al.19,20 increased this estimate to 9 (5–13)%, in agreement with our river-only estimate (9–11%), by explicitly simulating the nitrogen cycle. As opposed to riverine sustained NPP, no previous estimate exists for Arctic Ocean NPP sustained by coastal erosion. However, our estimates suggest that coastal erosion sustains a significantly larger part of Arctic Ocean NPP than rivers.

### An increasingly complex N-cycle in the Arctic

Several nonterrigenous sources and sinks of nitrogen in the Arctic Ocean are not considered in this study, e.g. nitrogen input from melting Greenland glaciers, atmospheric deposition, di-nitrogen fixation, and nitrogen losses through benthic denitrification. The inorganic nitrogen flux from Greenland glaciers is estimated to be of the same order of magnitude as riverine inorganic nitrogen, e.g. 0.3 Tg N yr−157. However, this flux is mainly directed into the CAA, the Nordic Seas, and the Labrador Seas from where they flow southward and not northward into the Arctic Ocean. Atmospheric deposition of nitrogen is estimated at approximately 0.1 Tg N yr−1 over the Arctic Ocean area without perennial sea-ice cover58 and is thus small compared to terrigenous nitrogen inputs. Similarly, nitrogen fixation has long been believed to be negligible in the Arctic Ocean due to low temperatures. However, recent studies in the Western Arctic challenge this view59,60 and estimate a maximum potential for Arctic Ocean nitrogen fixation of 3.5–9.2 Tg N yr−1 if this process was similar in all ice-free Arctic seas60. However, this potential pan-Arctic nitrogen fixation flux is of the same order as denitrification in Arctic sediments (2.8–29.0 Tg N yr−1)61,62, which is not represented in the model either. Thus, not simulating nitrogen fixation might offset the effect of not simulating denitrification in sediments, although we recognise that these two processes might be partly decoupled in space and time. However, the remarkably good spatial agreement between remote-sensing-based and simulated NPP (Fig. 3) suggests that, despite not taking into account all nonterrigenous sources and sinks of nitrogen, our model set-up represents the Arctic Ocean nitrogen cycle and NPP rather well.

In conclusion, this study provides a combined estimate of terrigenous nutrient fluxes into the Arctic from rivers and coastal erosion resolved in space and time and an estimate of the impact of these fluxes on Arctic Ocean NPP. Our finding that nutrient fluxes from coastal erosion are likely larger than riverine fluxes supports the previously hypothesised importance of coastal erosion for Arctic Ocean NPP and the dependent ecosystem13. However, the still large uncertainties with respect to the terrigenous fluxes and their respective lability highlight that more research is needed to better quantify the individual components of the Arctic Ocean nitrogen budget, in particular at the land-sea interface.

Despite all uncertainties, our results indicate that terrigenous nitrogen fluxes sustain 28–51% of Arctic Ocean NPP and suggest that coastal erosion is one of the main drivers of the Arctic Ocean NPP. Therefore, increases in Arctic Ocean NPP over the last decades6,7,63 that were exclusively attributed to decreasing sea-ice extent, a longer growing season, and ocean circulation changes may as well be partly caused by increases in riverine discharge64 and coastal erosion13,30. Moreover, terrigenous nitrogen input will likely increase over the 21st century13,16,65 and thus further increase Arctic Ocean NPP14. It is therefore of great importance that the terrigenous nutrient fluxes are better constrained and that they are consistently implemented in Earth System Models to improve the highly uncertain projections of Arctic Ocean NPP8 and the associated fishery catch potential over the 21st century9.

## Methods

### Arctic Ocean

In this study, we define the Arctic Ocean with the Fram Strait, the Barents Sea Opening, the Bering Strait, and the Baffin Bay as boundaries (Supplementary Fig. 2)66.

### Pan-Arctic extrapolation of river flux measurements

We derived a new forcing file representing a climatology of average monthly river fluxes of alkalinity (here assumed to represent entirely carbonate alkalinity, AC), dissolved inorganic carbon (CT), dissolved organic carbon (DOC), dissolved inorganic nitrogen (DIN), dissolved organic nitrogen (DON), total dissolved phosphorus (TDP), and silicic acid (SiT). This dataset is consistent with monthly data of coastal river discharge67. To do so, the observation-based flux estimates determined over the first decade of the 21st century from the six largest Arctic rivers (Mackenzie, Yukon, Kolyma, Lena, Ob, Yenisei) from the Arctic Great River Observatory (ArcticGRO) dataset12,21 were extrapolated to all river watersheds draining to coastal stretches north of 60°N latitude, using the STN30p stream network68 for delineation. Although the Yukon river does not drain directly into the Arctic Ocean, its large drainage basin lies predominantly north of 60°N and is representative of other ungauged Arctic rivers that drain directly into the Arctic Ocean.

First, the annual fluxes were spatially extrapolated to obtain an optimised estimate with regard to the total annual fluxes. Then, the annual fluxes were redistributed over the seasonal cycle using an empirical approach. By predicting the average annual fluxes (prediction of spatial variability only) first, these fluxes have lower uncertainty in the flux predictions than if spatial and seasonal variability had been predicted at the same time. Note that for the N-budget and NPP calculations for the Arctic Ocean, the mean average annual riverine input fluxes are of highest importance, and it is thus our priority to make the predicted mean annual fluxes as reliable as possible. The seasonal distribution of these fluxes over the year are of subordinate importance.

To identify potential predictors of the average annual fluxes of carbon and nutrients to the coast, a variety of catchment properties from available geodata were calculated (Supplementary Table 1 and Supplementary Fig. 6). Multiple linear regression was applied to extrapolate the annual river fluxes of the different carbon and nutrient species. For each of the carbon and nutrient species, the four predictors which best explained the differences between the six largest Arctic rivers, i.e. which gave the lowest root mean squared error (RMSE) between observed and predicted fluxes, were identified (Supplementary Table 2).

For CT and AC fluxes statistical models based on the same dataset of observed fluxes were previously developed by Tank et al.21 and use as predictors the carbonate index, the areal extent of permafrost, the areal proportion of glaciers, and runoff. We decided to use the same statistical models and geodata sets of predictors as Tank et al., but refitted the equations to account for slightly different river basin averages of the predictors that we calculated. While observed annual runoff from the six rivers was used to fit the regression, a global runoff dataset69 was used to extrapolate CT and AC fluxes to all boreal and Arctic rivers on the Northern Hemisphere following Tank et al. In order to obtain fluvial CT and AC fluxes that are consistent with the river discharge used as forcing data in the ocean-biogeochemical model NEMO-PISCES67, CT and AC concentrations were calculated by dividing the extrapolated annual fluxes by the annual runoff69. These concentrations were then multiplied with the here used river discharge67.

For DOC and dissolved nutrients, for which no statistical models existed beforehand, multiple linear regression was used to predict concentrations directly, testing all possible combinations of four predictors (Supplementary Table 2). For DOC, DON, DIN and TDP, the retained predictors were the areal extent of permafrost, the areal proportion of lakes, as well as the average clay and organic carbon contents of the topsoil. To avoid unreasonable numbers for extrapolated carbon and nutrient concentrations, the maximum and minimum flux weighted annual concentrations from the ArcticGRO data were imposed as upper and lower bounds for our extrapolation (Supplementary Table 3). The so-obtained concentrations were then multiplied by the river discharge used as forcing data in the ocean-biogeochemical model PISCES67 to obtain DOC and dissolved riverine nutrients fluxes.

In a next step, the average monthly fluxes were estimated based on the empirical relationship between the relative seasonal variations in matter fluxes and in river discharge:

$$F_{{\mathrm{monthly}}} = F_{{\mathrm{annual}}}a_1\left( {\frac{{Q_{{\mathrm{monthly}}}}}{{Q_{{\mathrm{annual}}}}}} \right)^{a_2}$$
(1)

with Fmonthly and Fannual being the monthly and annual flux, Qmonthly and Qannual being the monthly and annual discharge, and a1 and a2 being fitted parameters (Supplementary Table 4). Only for DIN, the position of each month in the seasonal cycle was used as an additional predictor:

$$F_{{\mathrm{monthly}}} = F_{{\mathrm{annual}}}\left[ {a_1\left( {\frac{{Q_{{\mathrm{monthly}}}}}{{Q_{{\mathrm{annual}}}}}} \right)^{a_2} \,+\, b_1{\mathrm{sin}}\left( {\frac{{b_2 + {\mathrm{month}}}}{6}\pi } \right)} \right]$$
(2)

with b1 and b2 being additional fitting parameters (Supplementary Table 4). For species other than DIN, no statistically significant (p < 0.05) fit for this part of the equation could be obtained.

Note that the exponent a2 describes how concentrations in carbon and nutrients react to changes in discharge, with a2 < 1 indicating a decrease in concentrations with increasing discharge, i.e. a dilution effect, and a2 > 1 indicating an increase in concentrations with discharge, i.e. the so-called “flushing effect”. For CT, AC, silica, and DIN the fitted a2 values indicate a dilution effect, consistent with observations12,21. Accordingly, we predict highest DIN concentrations during winter, when discharge is lowest (winter baseflow). The additional seasonal component which we fitted for monthly DIN fluxes represents an additional decrease in DIN fluxes over summer, which is as well consistent with the finding that during summertime, primary production additionally decreases riverine DIN fluxes12. For DOC and DON, our fitted a2 values indicate a flushing effect, which means that the increase in river flow during spring/summer contributes over-proportionally to the annual riverine DOC and DON exports, again consistent with observations12.

To avoid unrealistic AC to CT ratios, we derived minimum and maximum observed ratios from the ArcticGRO data and imposed them on our monthly estimates of AC. The minimum and maximum possible AC (μeq L−1) to CT (μmol L−1) ratios were thus defined as 0.24 and 1.07, respectively. Finally, to obtain the best possible forcing dataset of fluvial matter fluxes to coastal waters, the observation-based monthly average concentrations from the ArcticGRO data were used to calculate monthly fluxes for the six largest Arctic rivers. Thus, the extrapolated concentrations were only used for the ungauged part of the Arctic watershed. The final forcing file is provided on a regular 1° grid.

### Calculation of pan-Arctic carbon and nutrient fluxes from coastal erosion

We derived a new forcing file representing a climatology of average monthly total organic carbon (TOC), total nitrogen (TN), and total phosphorus (TP) fluxes from coastal erosion to the Arctic Ocean. First, TOC fluxes from coastal erosion were calculated by multiplying spatially resolved estimates of coastal erosion rates (based on observations from 1950 to 2010) by estimates of carbon content in coastal soils30. Then nitrogen fluxes were estimated by assuming a stoichiometric C:N ratio of 15.1:1.0 for the North American coast29 and 10.5:1.0 for the Eurasian coast28. Eventually, the phosphorus fluxes were calculated based on a global estimate of the soil N:P ratio of 13.1:131.

The obtained annual fluxes were then seasonally divided (2% in May, 5% in June, 15% in July, 29% in August and September, 15% in October, 5% in November) based on observations of coastal erosion rates70,71,72,73. The final forcing file is provided on a regular 1° grid, consistent with the forcing of riverine carbon and nutrient inputs.

### Ocean-biogeochemical model NEMO-PISCES

To analyse the effect of the riverine delivery of carbon and nutrients on the Arctic Ocean biogeochemistry, we used the version 3.2 of the ocean modelling framework’Nucleus for European Modelling of the Ocean’ (NEMO). This framework includes the ocean dynamics part OPA74, the version 2 of the Louvain-La-Neuve sea Ice Model LIM75 and the’Pelagic Interaction Scheme for Carbon and Ecosystem Studies’ (PISCES) biogeochemical model32. The model was used with the eddy admitting DRAKKAR configuration ORCA02576.

The biogeochemical model PISCES32 simulates the cycles of dissolved inorganic and organic carbon, total alkalinity, oxygen, nitrate (NO3), ammonium (NH4+), dissolved inorganic phosphate, silicic acid and iron. In addition, four living pools are simulated: nanophytoplankton and diatoms, and microzooplankton and mesozooplankton. The phytoplankton growth depends on temperature and is limited by light and nutrient availability. The photic depth reduces with increasing phytoplankton due to shading, whereas a possible shading from particles is not accounted for in the model. The C:N:P ratio of 122:16:177 is prescribed in all living and nonliving organic compartments of PISCES. In addition to the living compartments, PISCES simulates semi-labile dissolved organic matter (DOM), and small and big sinking organic particles.

External nutrient sources to the Arctic Ocean water column comprise lateral inflow from adjacent oceans, sediment remineralisation, river fluxes, and coastal erosion. The nutrient fluxes exchanged between the Arctic and the neighbouring oceans were calculated dynamically as the global model configuration was used. Sediment remineralisation is also calculated dynamically within the model. Nutrient fluxes from rivers and coastal erosion were calculated from the newly generated monthly 2-D forcing files. The fluxes from the regular 1° grid were rescaled to the curvilinear model grid. To do so, each model grid cell was assigned to its nearest grid cell on the 1° grid. The flux from the 1° grid was then divided between the assigned model grid cells, for coastal erosion in proportion to the surface area of each cell and for rivers in proportion to the runoff in each cell. This approach ensures the conservation of mass of the calculated fluxes and correlates runoff with carbon and nutrient fluxes. Vertically, the river input was divided on the first two vertical model grid levels (0–13 m) to account for a finite river depth.

### Land-ocean interface

All terrigenous fluxes were added to the respective inorganic ocean model variable (nitrogen was added in the form of nitrate), as the standard version of PISCES does not explicitly simulate DOC, DON and DOP separately. Instead, DON, DOP and DOC are simulated by a single tracer for semi-labile organic matter assuming a marine stoichiometric C:N:P ratio of 122:16:1. As opposed to this marine ratio, the stoichiometric C:N:P ratio in our estimated Arctic river fluxes is ~1188:25:112,21 and the C:N:P ratio in fluxes from coastal erosion is ~147:13:128,29,31. The configuration of PISCES does not allow to mix organic matter with different Redfield ratios. In order to conserve the total fluxes of carbon and nutrients, we chose to add all terrigenous organic matter fluxes to the ocean in their inorganic form, which is an overestimation that we quantify in the “Uncertainty estimation” section below.

### Simulation strategy

In this study, we ran three global simulations with the NEMO-PISCES model from 1990 to 2010: (1) one with the newly derived forcing dataset for terrigenous carbon and nutrient fluxes from rivers and coastal erosion (Referred to as Baseline), (2) one with coastal erosion fluxes set to zero (NoCoast), (3) one with coastal erosion fluxes and riverine carbon and nutrient fluxes set to zero (NoTerr). All three simulations were initialised in 1990 with the output from previously published simulations37 and ran with the same model parameters and external forcing, apart from the different input of terrigenous carbon and nutrients in the Arctic Ocean. The initialisation in 1990 from a simulation with different terrigenous carbon and nutrient input leads to a transient period that is visible in the annual Arctic Ocean NPP from 1990 to 2004 (Supplementary Fig. 7). Only model output after the transient period from 2005 to 2010 was analysed to ensure that the results are solely driven by the new terrigenous carbon and nutrient inputs.

### Uncertainty estimation

In this study, the uncertainties related to the quality of the forcing files and the uncertainties related to the lability of the terrigenous organic matter are separately quantified.

The estimated terrigenous carbon and nutrient fluxes have uncertainties due to the scarcity of the data in the difficult to sample Arctic environment and due to the extrapolation on the pan-Arctic scale. These uncertainties had to be estimated here because previously published observation-based river fluxes12,21 and erosion rates30 were given without uncertainties. The uncertainties for riverine carbon and nutrient fluxes arise mainly from the temporal and spatial extrapolation12. The uncertainty from temporal extrapolation was previously only estimated for CT fluxes (4%)21 and we assumed that this uncertainty is representative for DOC and nutrient fluxes12, too. To quantify the uncertainty due to the spatial extrapolation of the riverine fluxes, we relied on the range of previously reported extrapolations of riverine DOC exports to the Arctic watershed (25–30 Tg C yr−1)12,27,78, which also includes our own basin-wide annual riverine DOC flux of 27.6 Tg C yr−1. The uncertainty in both directions is thus estimated at about 10%, which combined with a temporal uncertainty of 4%, leads to a total, symmetric uncertainty for the riverine fluxes of carbon and nutrients of ±11%.

In comparison to river fluxes, the fluxes from coastal erosion have much higher uncertainties, mainly caused by uncertainties in the erosion rate in space and time, the soil organic carbon content, the C:N:P ratio in the soil, and the extrapolation of these measured quantities. Both, the previously published spatially extrapolated erosion rates and soil organic carbon content of the eroded material are reported without uncertainties30. In particular the soil carbon content varies strongly and has local maxima, which are often missed by low-resolution sampling79. Based on these spatial variations with localised maxima, we assume an asymmetric uncertainty for carbon coastal erosion fluxes of 30% towards lower values and 50% towards higher values. For nutrient fluxes, the C:N:P ratio adds another source of uncertainty. To constrain this uncertainty, we use the standard deviation of the C:N:P ratio among existing measurements, which is 27% for the C:N ratio28,29 and 6% for the P:N ratio, which is derived from global estimates31. We thus obtain a relative uncertainty range from −40 to +57% for organic N fluxes and −41 to +57% for organic P fluxes from coastal erosion, which are larger than for the riverine fluxes.

The lability of the organic matter flux adds another source of uncertainty, which is assessed in the following way. For rivers, estimates of lability of riverine organic matter in the Arctic Ocean vary strongly from 20–40% of riverine DOC from Alaskan rivers being remineralised within three months24, over 50% of terrigenous DOC on the Siberian shelf being remineralised within a year49, to 62–76% of riverine DON on the Siberian shelf being remineralised within in couple of months50. Taking into account that residence times on the Siberian shelves reach 3.5 ± 2 years53 and even 10 years in the Canada basin54, it was estimated that a large fraction of the terrigenous organic carbon will be remineralised within the Arctic Ocean, in agreement with the finding that only 21–34% of the riverine organic carbon is leaving the Arctic Ocean48. Our study thus likely overestimates the amount of the NPP fuelling, labile DON pool. Based on the available studies, we thus estimate 20–80% of the DON flux to be labile.

The organic matter from coastal erosion is expected to be even more reactive than riverine supplies, in agreement with the findings that thawing permafrost soils release one of the most labile forms of organic matter in nature80,81,82. Observation-based estimates of remineralisation rates of terrigenous organic matter in the Laptev Sea and East-Siberian Sea are 0.87 Tg N yr−1 in sediments52 and 0.38 Tg N yr−1 in the water column51. Scaled up to the entire Arctic Ocean, using the primary production sustained by terrigenous nutrients as scaling factor, remineralisation rates of 1.56 Tg N yr−1 in sediments and 0.68 Tg N yr−1 in the water column are obtained. Compared to our estimated input of organic nitrogen from rivers and coastal erosion (2.37 Tg N yr−1), this yields a remineralisation rate of 95%. The almost complete remineralisation of terrigenous organic matter contradicts the observations of strong, but quantitatively uncertain sedimentation in the coastal Arctic29,47,55,56. The apparent mismatch between organic matter input and remineralisation might be due to missing sources of terrigenous matter in our study, e.g. subsea coastal erosion16 or the riverine particulate matter22 that does not precipitate in the river delta33 or due to resuspension of terrestrial organic matter in the nearshore zone34,56. Following the observed remineralisation rates for terrigenous organic carbon51,52 in sediments and the water column, we estimate that 80 (70–90)% of our estimated input of organic nutrients released by coastal erosion will contribute to NPP before leaving the shelf seas.

### Remote-sensing-based NPP estimates

NPP was compared to estimates derived from remotely sensed ocean color from 2005 to 20106,11. Remote-sensing-based NPP is estimated from satellite observations of chlorophyll using an algorithm that was calibrated with in-situ observations of chlorophyll-a. The reported uncertainties (Table 2) are calculated as the standard deviation of annual NPP from 2005 to 2010.

## Data availability

The spatially resolved input of nitrogen from coastal erosions and rivers and the model output that supports the findings of this study are available under https://doi.org/10.17882/76983.

## Code availability

The model code is publicly available at https://www.nemo-ocean.eu/.

## References

1. 1.

Bluhm, B. A. & Gradinger, R. Regional variability in food availability for Arctic marine mammals. Ecol. Appl. 18, 77–96 (2008).

2. 2.

Kattner, G. & Budéus, G. Nutrient status of the northeast water polynya. J. Mar. syst. 10, 185–197 (1997).

3. 3.

Simpson, K. G., Tremblay, J ‐ É., Gratton, Y. & Price, N. M. An annual study of inorganic and organic nitrogen and phosphorus and silicic acid in the southeastern Beaufort Sea, J. Geophys. Res. 113, C07016 (2008).

4. 4.

Tremblay, J. E. et al. Global and regional drivers of nutrient supply, primary production and CO2 drawdown in the changing Arctic Ocean. Prog. Oceanogr. 139, 171–196 (2015).

5. 5.

Meredith, M. & Sommerkorn, M. IPCC Special Report on the Ocean and Cryosphere in a Changing Climate (SROCC), Chapter 3 (IPCC, Geneva, Switzerland, 2019).

6. 6.

Arrigo, K. R. & van Dijken, G. L. Continued increases in Arctic Ocean primary production. Progr. Oceanogr. 136, 60–70 (2015).

7. 7.

Lewis, K. M., van Dijken, G. L. & Arrigo, K. R. Changes in phytoplankton concentration now drive increased Arctic Ocean primary production. Science 369, 198–202 (2020).

8. 8.

Vancoppenolle, M. et al. Future Arctic Ocean primary productivity from CMIP5 simulations: uncertain outcome, but consistent mechanisms. Glob. Biogeochem. Cycles 27, 605–619 (2013).

9. 9.

Cheung, W. W. L. & Reygondeau, G. Large benefits to marine fisheries of meeting the 1.5 °C global warming target. Science 354, 1591–1594 (2016).

10. 10.

Popova, E. E. et al. What controls primary production in the Arctic Ocean? Results from an intercomparison of five general circulation models with biogeochemistry. J. Geophys. Res. 117, C00D12 (2012).

11. 11.

Arrigo, K. R. & van Dijken, G. L. Secular trends in Arctic Ocean net primary production. J. Geophys. Res. 116, 1527–1540 (2011).

12. 12.

Holmes, R. M. et al. Seasonal and annual fluxes of nutrients and organic matter from large rivers to the Arctic ocean and surrounding seas. Estuar. Coast. 35, 369–382 (2011).

13. 13.

Fritz, M., Vonk, J. E. & Lantuit, H. Collapsing Arctic coastlines. Nat. Clim. Change 7, 6–7 (2017).

14. 14.

Terhaar, J., Orr, J. C., Ethé, C., Regnier, P., & Bopp, L. Simulated Arctic Ocean response to doubling of riverine carbon and nutrient delivery. Glob, Biogeochem. Cycles 33, 1048–1070 (2019).

15. 15.

McClelland, J. W., Holmes, R. M., Dunton, K. H. & Macdonald, R. W. The Arctic Ocean estuary. Estuaries Coasts 35, 353–368 (2011).

16. 16.

Vonk, J. E. et al. Activation of old carbon by erosion of coastal and subsea permafrost in Arctic Siberia. Nature 489, 137–140 (2012).

17. 17.

Wegner, C. et al. Variability in transport of terrigenous material on the shelves and the deep Arctic Ocean during the Holocene. Polar Res. 34, https://doi.org/10.3402/polar.v%v.24964 (2015).

18. 18.

Tank, S. E., Manizza, M., Holmes, R., McClelland, J. W. & Peterson, B. J. The processing and impact of dissolved riverine nitrogen in the Arctic Ocean. Estuaries Coasts 35, 401–415 (2012).

19. 19.

Le Fouest, V., Babin, M. & Tremblay, J.-É. The fate of riverine nutrients on Arctic shelves. Biogeosciences 10, 3661–3677 (2013).

20. 20.

Le Fouest, V. et al. Modelling the impact of riverine DON removal by marine bacterioplankton on primary production in the Arctic Ocean. Biogeosciences 12, 3385–3402 (2015).

21. 21.

Tank, S. E. et al. A land‐to‐ocean perspective on the magnitude, source and implication of DIC flux from major Arctic rivers to the Arctic Ocean. Glob. Biogeochem. Cycles, 26, GB4018 (2012).

22. 22.

McClelland, J. W. et al. Particulate organic carbon and nitrogen export from major Arctic rivers. Glob. Biogeochem. Cycles 30, 629–643 (2016).

23. 23.

Holmes, R. M. et al. Flux of nutrients from Russian rivers to the Arctic Ocean: can we establish a baseline against which to judge future changes. Water Resour. Res. 36, 2309–2320 (2000).

24. 24.

Holmes, R. M. et al. Lability of DOC transported by Alaskan rivers to the Arctic Ocean. Geophys. Res. Lett. 35, L03402 (2008).

25. 25.

McClelland, J. W. et al. River export of nutrients and organic matter from the North Slope of Alaska to the Beaufort Sea. Water Resour. Res. 50, 1823–1839 (2014).

26. 26.

Li Yung Lung, J. Y. S. et al. Seasonal and geographic variation in dissolved carbon biogeochemistry of rivers draining to the Canadian Arctic Ocean and Hudson Bay. J. Geophys. Res. 123, 3371–3386 (2018).

27. 27.

Manizza, M. et al. Modeling transport and fate of riverine dissolved organic carbon in the Arctic Ocean. Glob. Biogeochem. Cycles 23, GB4006 (2009).

28. 28.

Schirrmeister, L. et al. Sedimentary characteristics and origin of the Late Pleistocene Ice Complex on north-east Siberian Arctic coastal lowlands and islands—a review. Quat. Int. 241, 3–25 (2011).

29. 29.

Couture, N. J., Irrgang, A., Pollard, W., Lantuit, H. & Fritz, M. Coastal erosion of permafrost soils along the Yukon Coastal Plain and fluxes of organic carbon to the Canadian Beaufort Sea. J. Geophys. Res. 123, 406–422 (2018).

30. 30.

Lantuit, H. et al. The Arctic Coastal Dynamics database: a new classification scheme and statistics on Arctic permafrost coastlines. Estuaries Coasts 35, 383–400 (2012).

31. 31.

Cleveland, C. C. & Liptzin, D. C:N:P stoichiometry in soil: is there a “Redfield ratio” for the microbial biomass? Biogeochemistry 85, 235–252 (2006).

32. 32.

Aumont, O. & Bopp, L. Globalizing results from ocean in situ iron fertilization studies. Glob. Biogeochem. Cycles 20, GB2017 (2006).

33. 33.

Semiletov, I. P. et al. Carbon transport by the Lena River from its headwaters to the Arctic Ocean, with emphasis on fluvial input of terrestrial particulate organic carbon vs. carbon transport by coastal erosion. Biogeosciences 8, 2407–2426 (2011).

34. 34.

Tanski, G., Couture, N., Lantuit, H., Eulenburg, A. & Fritz, M. Eroding permafrost coasts release low amounts of dissolved organic carbon (DOC) from ground ice into the nearshore zone of the Arctic Ocean. Glob. Biogeochem. Cycles 30, 1054–1068 (2016).

35. 35.

Jones, B. M. et al. Increase in the rate and uniformity of coastline erosion in Arctic Alaska. Geophys. Res. Lett. 36, L03503 (2009).

36. 36.

Rachold, V. et al. in The Organic Carbon Cycle in the Arctic Ocean, pp. 33–55 (Springer, Berlin, 2004).

37. 37.

Terhaar, J., Orr, J. C., Gehlen, M., Ethé, C. & Bopp, L. Model constraints on the anthropogenic carbon budget of the Arctic Ocean. Biogeosciences 16, 2343–2367 (2019).

38. 38.

Semiletov, I. et al. The East Siberian Sea as a transition zone between Pacific-derived waters and Arctic shelf waters. Geophys. Res. Lett. 32, L10614 (2005).

39. 39.

Torres-Valdes, S. et al. Export of nutrients from the Arctic Ocean. J. Geophys. Res 118, 1625–1644 (2013).

40. 40.

Smith, W. Jr et al. New production in the Northeast Water Polynya: 1993. J. Mar. Syst. 10, 199–209 (1997).

41. 41.

Tremblay, J. E., Michel, C., Hobson, K. A., Gosselin, M. & Price, N. M. Bloom dynamics in early opening waters of the Arctic Ocean. Limnol. Oceanogr. 51, 900–912 (2006).

42. 42.

Garneau, M. È., Gosselin, M., Klein, B., Tremblay, J. É. & Fouilland, E. New and regenerated production during a late summer bloom in an Arctic polynya. Mar. Ecol. Prog. Ser. 345, 13–26 (2007).

43. 43.

Emmerton, C. A., Lesack, L. F. W. & Vincent, W. F. Mackenzie River nutrient delivery to the Arctic Ocean and effects of the Mackenzie Delta during open water conditions. Glob. Biogeochem. Cycles 22, GB1024 (2008).

44. 44.

Shi, W. & Wang, M. Characterization of global ocean turbidity from Moderate Resolution Imaging Spectroradiometer ocean color observations. J. Geophys. Res. 115, C11022 (2010).

45. 45.

Klein, K. P. et al. Long-term high-resolution sediment and sea surface temperature spatial patterns in Arctic nearshore waters retrieved using 30-year landsat archive imagery. Remote Sens. 11, 2791 (2019).

46. 46.

Wegner, C. et al. Suspended particulate matter on the Laptev Sea shelf (Siberian Arctic) during ice-free conditions. Estuar. Coast. Shelf S. 57, 55–64 (2003).

47. 47.

Jong, D. et al. Nearshore zone dynamics determine pathway of organic carbon from eroding permafrost coasts. Geophys. Res. Lett. 47, e2020GL088561 (2020).

48. 48.

Hansell, D. A., Kadko, D. & Bates, N. R. Degradation of terrigenous dissolved organic carbon in the western Arctic Ocean. Science 304, 858–861 (2004).

49. 49.

Kaiser, K., Benner, R. & Amon, R. The fate of terrigenous dissolved organic carbon on the Eurasian shelves and export to the North Atlantic. J. Geophys. Res. 122, 4–22 (2017).

50. 50.

Thibodeau, B., Bauch, D. & Voss, M. Nitrogen dynamic in Eurasian coastal Arctic ecosystem: Insight from nitrogen isotope. Glob. Biogeochem. Cycles 31, 836–849 (2017).

51. 51.

Sánchez-García, L. et al. Inventories and behaviour of particulate organic carbon in the Laptev and East Siberian seas. Glob. Biogeochem. Cycles 25, GB2007 (2011).

52. 52.

Brüchert, V. et al. Carbon mineralization in Laptev and East Siberian sea shelf and slope sediment. Biogeosciences 15, 471–490 (2018).

53. 53.

Schlosser, P., Bauch, D., Fairbanks, R. & Bönisch, G. Arctic river-runoff: mean residence time on the shelves and in the halocline. Deep Sea Res. Part I 41, 1053–1068 (1994).

54. 54.

Fichot, C. G. et al. Pan-Arctic distributions of continental runoff in the Arctic Ocean. Sci. Rep. 3, 1–6 (2013).

55. 55.

Hilton, R. et al. Erosion of organic carbon in the Arctic as a geological carbon dioxide sink. Nature 524, 84–87 (2015).

56. 56.

Grotheer, H. et al. Burial and origin of permafrost‐derived carbon in the nearshore zone of the southern Canadian Beaufort Sea. Geophys. Res. Lett. 47, e2019GL085897 (2020).

57. 57.

Wadham, J. L. et al. Sources, cycling and export of nitrogen on the Greenland Ice Sheet. Biogeosciences 13, 6339–6352 (2016).

58. 58.

Lamarque, J. F. et al. Multi-model mean nitrogen and sulfur deposition from the Atmospheric Chemistry and Climate Model Intercomparison Project (ACCMIP): evaluation of historical and projected future changes. Atmos. Chem. Phys. 13, 7997–8018 (2013).

59. 59.

Harding, Katie et al. Symbiotic unicellular cyanobacteria fix nitrogen in the Arctic Ocean. Proc. Natl Acad. Sci. USA 115, 13371–13375 (2018).

60. 60.

Sipler, R. E. et al. Preliminary estimates of the contribution of Arctic nitrogen fixation to the global nitrogen budget. Limnol. Oceanogr. Lett. 2.5, 159–166 (2017).

61. 61.

Chang, B. X. & Devol, A. H. Seasonal and spatial patterns of sedimentary denitrification rates in the Chukchi sea. Deep Sea Res. Part II 56, 1339–1350 (2009).

62. 62.

McTigue, N. et al. Biotic and abiotic controls on co-occurring nitrogen cycling processes in shallow Arctic shelf sediments. Nat. Commun. 7, 13145 (2016).

63. 63.

Arrigo, K. R., van Dijken, G. & Pabi, S. Impact of a shrinking arctic ice cover on marine primary production. Geophys. Res. Lett. 35, L19603 (2008).

64. 64.

McClelland, J. W., Déry, S. J., Peterson, B. J., Holmes, R. M. & Wood, E. F. A pan-Arctic evaluation of changes in river discharge during the latter half of the 20th century. Geophys. Res. Lett. 33, L06715 (2006).

65. 65.

Frey, K. E., McClelland, J. W., Holmes, R. M. & Smith, L. C. Impacts of climate warming and permafrost thaw on the riverine transport of nitrogen and phosphorus to the Kara Sea. J. Geophys. Res. 112, G04S58 (2007).

66. 66.

Bates, N. R. & Mathis, J. T. The Arctic Ocean marine carbon cycle: evaluation of air-sea CO2 exchanges, ocean acidification impacts and potential feedbacks. Biogeosciences 6, 2433–2459 (2009).

67. 67.

Dai, A. & Trenberth, K. E. Estimates of freshwater discharge from continents: latitudinal and seasonal variations. J. Hydrometeorol. 3, 660–687 (2002).

68. 68.

Vörösmarty, C. J., Green, P., Salisbury, J. & Lammers, R. B. Global water resources: vulnerability from climate change and population growth. Science 289, 284–288 (2000).

69. 69.

Fekete, B. M., Vörösmarty, C. J. & Grabs, W. High-resolution fields of global runoff combining observed river discharge and simulated water balances. Glob. Biogeochem. Cycles 16, 15-1–15-10 (2002).

70. 70.

Jones, B. M. et al. Increase in the rate and uniformity of coastline erosion in Arctic Alaska. Geophys. Res. Lett. 36, L03503 (2009).

71. 71.

Wobus, C. et al. Thermal erosion of a permafrost coastline: improving process-based models using time-lapse photography. Arc. AntArc. Alp. Res. 43, 474–484 (2011).

72. 72.

Barnhart, K. R. et al. Modeling erosion of ice-rich permafrost bluffs along the Alaskan Beaufort Sea coast. J. Geophys. Res. 119, 1155–1179 (2014).

73. 73.

Günther, F. et al. Observing Muostakh disappear: permafrost thaw subsidence and erosion of a ground-ice-rich island in response to arctic summer warming and sea ice reduction. Cryosphere 9, 151–178 (2015).

74. 74.

Madec, G. NEMO Ocean Engine (Note du Pôle de Modélisation, Institut Pierre-Simon Laplace, 2008).

75. 75.

Fichefet, T. & Morales Maqueda, M. A. Sensitivity of a global sea ice model to the treatment of ice thermodynamics and dynamics. J. Geophys. Res. 102, 12609–12646 (1997).

76. 76.

Barnier, B. et al. Impact of partial steps and momentum advection schemes in a global ocean circulation model at eddy permitting resolution. Ocean Dyn. 56, 543–567 (2006).

77. 77.

Takahashi, T., Broecker, W. S. & Langer, S. Redfield ratio based on chemical data from isopycnal surfaces. J. Geophys. Res. 90, 6907–6924 (1985).

78. 78.

Raymond, P. A. et al. Flux and age of dissolved organic carbon exported to the Arctic Ocean: a carbon isotopic study of the five largest arctic rivers. Glob. Biogeochem. Cycles 21, GB4011 (2007).

79. 79.

Tarnocai, C. et al. Soil organic carbon pools in the northern circumpolar permafrost region. Glob. Biogeochem. Cycles 23, GB2023 (2009).

80. 80.

Sánchez‐García, L. et al. Characterisation of three regimes of collapsing Arctic ice complex deposits on the SE Laptev Sea coast using biomarkers and dual carbon isotopes. Permafr. Periglac. 25, 172–183 (2014).

81. 81.

Vonk, J. E. et al. High biolability of ancient permafrost carbon upon thaw. Geophys. Res. Lett. 40, 2689–2693 (2013).

82. 82.

Mann, P. J. et al. Utilization of ancient permafrost carbon in headwaters of Arctic fluvial networks. Nat. Commun. 6, 7856 (2015).

## Acknowledgements

This study has received funding from the European Union’s Horizon 2020 research and innovation programme under grant agreement No 643052 (C-CASCADES), No 641816 (CRESCENDO), No 776810 (VERIFY) and No 821003 (4 C). The work reflects only the authors’ view; the European Commission and their executive agency are not responsible for any use that may be made of the information the work contains. This study has also received funding from the Agence Nationale de la Recherche grant ANR-18-ERC2-0001-01 (CONVINCE), the MTES/FRB Acidoscope project and the ENS-Chanel research chair. We also thank C. Ethé for help with the NEMO-PISCES simulations.

## Author information

Authors

### Contributions

J.T. and R.L. led the study. R.L. created the forcing files for terrigenous carbon and nutrients and J.T. the ocean-biogeochemical simulations. Model analysis and production of figures was done by J.T. with help from R.L., P.R., N.G. and L.B. The manuscript was drafted by J.T. and modified and improved by R.L., P.R., N.G. and L.B.

### Corresponding author

Correspondence to Jens Terhaar.

## Ethics declarations

### Competing interests

The authors declare no competing interests.

Peer review information Nature Communications thanks Michael Fritz and other, anonymous, reviewers for their contributions to the peer review of this work. Peer review reports are available.

Publisher’s note Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.

## Rights and permissions

Reprints and Permissions

Terhaar, J., Lauerwald, R., Regnier, P. et al. Around one third of current Arctic Ocean primary production sustained by rivers and coastal erosion. Nat Commun 12, 169 (2021). https://doi.org/10.1038/s41467-020-20470-z

• Accepted:

• Published:

• DOI: https://doi.org/10.1038/s41467-020-20470-z

• ### Drivers, dynamics and impacts of changing Arctic coasts

• Anna M. Irrgang
• Mette Bendixen
• Benjamin M. Jones

Nature Reviews Earth & Environment (2022)

• ### Seasonal nitrogen fluxes of the Lena River Delta

• Tina Sanders
• Claudia Fiencke
• Kirstin Dähnke

Ambio (2022)

• ### Oceanographic and biogeochemical drivers cause divergent trends in the nitrogen isoscape in a changing Arctic Ocean

• Pearse James Buchanan
• Alessandro Tagliabue
• Claire Mahaffey

Ambio (2022)

• ### Degrading permafrost river catchments and their impact on Arctic Ocean nearshore processes

• Paul J. Mann
• Jens Strauss
• Bennet Juhls

Ambio (2022)

• ### Nutrient pathways and their susceptibility to past and future change in the Eurasian Arctic Ocean

• Robyn E. Tuerena
• Claire Mahaffey
• Christian März

Ambio (2022)