# Key drivers of pyrogenic carbon redistribution during a simulated rainfall event

Severin-Luca Bellè, Asmeret Asefaw Berhe, Frank Hagedorn, Cristina Santin, Marcus Schiedung, Ilja van Meerveld, Samuel Abiven

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Severin-Luca Bellè, Asmeret Asefaw Berhe, Frank Hagedorn, Cristina Santin, Marcus Schiedung, et al. Key drivers of pyrogenic carbon redistribution during a simulated rainfall event. Biogeosciences, 2020, 27 (7), pp.1387-1407. 10.5194/bg-2020-361. hal-03986404

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# Key drivers of pyrogenic carbon redistribution during a simulated rainfall event

Severin-Luca Bellè<fnref n="1" />, Asmeret Asefaw Berhe<fnref n="2" />, Frank Hagedorn<fnref n="3" />, Cristina Santin<fnref n="4" />,<fnref n="5" />, Marcus Schiedung<fnref n="1" />, Ilja van Meerveld<fnref n="1" />, and Samuel Abiven<fnref n="1" />,<fnref n="6" />,<fnref n="7" />

**Correspondence:** Samuel Abiven (abiven@biotite.ens.fr)

Received: 30 September 2020 – Discussion started: 2 November 2020

Revised: 4 January 2021 – Accepted: 7 January 2021 – Published: 15 February 2021

**Abstract.** Pyrogenic carbon (PyC) is produced by the incomplete combustion of vegetation during wildfires and is a major and persistent pool of the global carbon (C) cycle. However, its redistribution in the landscape after fires remains largely unknown. Therefore, we conducted rainfall simulation experiments on 0.25 m<fnref n="2" /> plots with two distinct Swiss forest soils (Cambisol (clay loam) and Luvisol (sandy silt)). We applied PyC produced from wood (*Picea abies*) labeled under FACE conditions and C₄ grass (*Miscanthus sinensis*) to the soil surface to study PyC redistribution by runoff and splash and the vertical mobility of PyC in a 10 cm unsaturated soil column based on the differences in δ¹³C of soils and PyC. We assessed the effect of soil texture, slope angle and PyC characteristics (feedstock and particle size) on the mobility of PyC during 30 min of intense rainfall (102 mm h⁻<fnref n="1" />). Our results highlight that PyC is highly mobile. Surface runoff transported between 0.2 % and 36.0 % of the total added PyC. Erosion by splash further redistributed 10.3 % to 25.3 % of the added PyC. Soil type had a substantial impact on the redistribution of PyC by both runoff and splash: on average, we recovered 10.5 % of the added PyC in runoff and splashed material for the clay-rich Cambisol and 61.3 % of the added PyC for the sandy silt Luvisol combined.

PyC feedstock had a clear but contrasting effect on PyC redistribution: relocation in the runoff and splashed material was greater for wood PyC (43.4 % of total added PyC) than grass PyC (28.4 %). However, more wood PyC (11.5 %; fraction of organic C derived from the PyC) remained where it was initially applied compared to grass PyC (7.4 %). The results further suggest that the effect of PyC characteristics on its mobility can be highly variable and depend not only on the material from which it was derived, but also on other factors (e.g., particle size, porosity, density). In particular, the mobility of PyC was almost twice as large for fine-grained PyC (< 63 µm) than for coarse PyC (63 µm–2 mm). Vertical mobility of PyC up to 10 cm depth was greater in the clay-rich, well-aggregated Cambisol but limited in the physically instable Luvisol, likely due to quick aggregate breakdown and surface sealing. The addition of PyC to the surface of the studied soils further induced changes in the export of native soil organic carbon (nSOC) after the 30 min rainfall event. Our study shows that large quantities of PyC can be redistributed by water erosion over short timescales and that the mobility of PyC depends to a great extent on the response of soils to rainfall. Moreover, the addition and redistribution

<footnote n="1">¹Department of Geography, University of Zurich, Winterthurerstrasse 190, 8057 Zurich, Switzerland</footnote>

<footnote n="2">²School of Natural Sciences, University of California, Merced, CA 95340, USA</footnote>

<footnote n="3">³Forest soils and Biogeochemistry, Swiss Federal Research Institute WSL, Zürcherstrasse 111, 8903 Birmensdorf, Switzerland</footnote>

<footnote n="4">⁴Department of Biosciences, College of Science, Swansea University, Swansea, UK</footnote>

<footnote n="5">⁵Research of Biodiversity (CSIC, UO, PA), University of Oviedo, Mieres, Spain</footnote>

<footnote n="6">⁶Laboratoire de Géologie, Département de Géosciences, CNRS – École normale supérieure, PSL University, Institut Pierre Simon Laplace, Rue Lhomond 24, 75005 Paris, France</footnote>

<footnote n="7">⁷CEREEP-Ecotron Ile De France, ENS, CNRS, PSL University, Chemin de busseau 11, 77140 St-Pierre-lès-Nemours, France</footnote>
of PyC affects the export of nSOC and thus the C budget of fire-affected soils and catchments.

# 1 Introduction

Wildfires burn 345 to 464 Mha, i.e., 4% of vegetated land area, annually and are thus a major disturbance for terrestrial ecosystems (Giglio et al., 2013; Randerson et al., 2012). The associated carbon (C) flux of 2.2 Pg to the atmosphere affects the global C cycle and the Earth's climate (Bowman et al., 2009; van der Werf et al., 2017). It is predicted that fire frequencies will increase in many regions around the world due to climate change. This amplifies the importance of fires for key biogeochemical and climate processes and its correct representation in Earth system models (Conard and Solomon, 2008; Lasslop et al., 2019; Westerling et al., 2006). In addition to the impact on atmospheric C emissions, wildfires also affect the global C cycle through the impact on the Earth's surface processes (Lasslop et al., 2019). The incomplete combustion of vegetation during fires produces a continuum of C-rich materials with polycyclic, condensed aromatic molecular structures, ranging from soot to macroscopic charcoal (Bird et al., 2015; Hammes and Abiven, 2013). The global production of this fire-derived or pyrogenic C (PyC) is estimated to be 192 to 340 Tg PyC annually (Jones et al., 2019; Santín et al., 2016). PyC is environmentally more resistant than its unburnt precursors and can remain in terrestrial and aquatic ecosystems for decades to millennia (Abiven and Santín, 2019; Coppola and Druffel, 2016; Santín et al., 2016). It is one of the largest and oldest C pools on Earth (Bird et al., 2015) and globally accounts for around 15% of organic carbon (OC) in soils (Reisser et al., 2016). However, we currently have little knowledge about the fate of PyC in the landscape, and the dominant processes that lead to its mobilization, degradation and stabilization at different landscape positions and at the interface between land and ocean still need to be clarified (Abiven and Santín, 2019; Abney and Berhe, 2018; Masiello and Berhe, 2020).

Erosion by water represents a fundamental transport process for soil organic carbon (SOC) and PyC in terrestrial sloping landscapes and determines its export to aquatic systems (Abney and Berhe, 2018; Berhe et al., 2018). Water erosion refers here to the detachment of particles by raindrop impact, subsequent transport by water and final deposition (Berhe et al., 2018; Doetterl et al., 2016). It takes place as splash erosion, interrill erosion, and rill-gully erosion (de Nijs and Cammeraat, 2020). Erosion globally causes the redistribution of 10 to 140 Pg of soil per year (Berhe et al., 2018; Doetterl et al., 2016). Estimates of global SOC erosion range between 0.3 and 5 Pg yr⁻¹ (Berhe et al., 2007; Chappell et al., 2016; Lal, 2004; Stallard, 1998). For PyC it has been estimated to be between 3 and 5 Tg yr⁻¹ based on field investigations in Mediterranean climate (Abney et

al., 2017) and 29 to 87 Tg yr⁻¹ based on modeling of global PyC dynamics (Bird et al., 2015). The diverse methods used to quantify PyC contribute to the large variability in reported values of PyC erosion. Physical (based on size and density of PyC), chemical (based on the oxidation resistance of PyC), thermal (based on temperature resistance of PyC), spectroscopic (based on magnetic or photonic response of PyC to input signal) and molecular marker (based on identification of PyC specific compounds) methods cover different windows of the PyC continuum, and, therefore, estimates of PyC movement in the landscape can vary substantially (Bird et al., 2015; Hammes and Abiven, 2013).

Erosion by water can have a profound impact on the persistence and fate of SOC and PyC as it can transfer these forms of OC from eroding landscapes to depositional sites where they can be preserved for a long time (Abney et al., 2017; Abney and Berhe, 2018). However, it can also accelerate decomposition of SOC and PyC by physical disintegration (Abney et al., 2019b; Pignatello et al., 2015) and biochemical degradation during and after transport (Hilscher and Knicker, 2011; Singh et al., 2012). Although it was debated in the past if erosion by water is a net C sink or source (Doetterl et al., 2016), it is today considered to be a C sink. However, the size of the erosion-induced C sink still needs to be assessed (Abney and Berhe, 2018; Berhe et al., 2018).

In post-fire landscapes erosion by water is very often substantially enhanced (Abney and Berhe, 2018; Masiello and Berhe, 2020; Vieira et al., 2018). The removal of the protective vegetation cover during wildfires increases the impact of raindrops on the soil surface (Certini, 2005; Johansen et al., 2001; Pierson et al., 2013), which can cause aggregate breakdown and surface sealing (Moody et al., 2013; Shakesby, 2011). The effects of fire-induced changes on the structural and hydrological properties of soils and erosion depend on the fire regime (frequency, severity, intensity and extent), precipitation pattern (timing, frequency, intensity, watershed hydrology), vegetation (fuel load, ground cover, regrowth dynamics), topography (slope steepness, aspect, and length, micro-topography) and soil properties (texture, aggregation, saturation) (Abney and Berhe, 2018; Archibald et al., 2013; Berhe et al., 2012; Moody et al., 2013; Rumpel et al., 2015; Shakesby and Doerr, 2006). Soil type determines the extent to which erodible materials are susceptible to detachment and mobilization and, together with the local geomorphology, governs soil physical stability and therefore erodibility (Moody et al., 2013; Vieira et al., 2015).

The PyC particles produced during a fire that remain on the soil surface may be more redistributed by water erosion during the first rainfall than other soil particles (Abney et al., 2019a; Rumpel et al., 2006, 2009). This high mobilization of PyC is partially caused by its physical properties, in particular its low density and high porosity, but also due to the lack of organo-mineral interactions between the PyC and soil matrix that prevent either washout (surface erosion by interrill or splash) or washin (to deeper soil horizons) during ini-
tial rainfall (Brewer et al., 2014; Masiello and Berhe, 2020; Pyle et al., 2017). Most PyC materials have a high initial hy-
drophobicity, which can promote floating and transport by
water (Abney and Berhe, 2018; Rumpel et al., 2015). The
transport of PyC also depends on the material from which it
was derived, with grass-derived PyC being perceived to be
more mobile than wood PyC (Saiz et al., 2018). Here, the
physical stability of PyC plays a role: PyC that can be frag-
mented more easily will produce smaller particles (Pignatello
et al., 2015; Saiz et al., 2018) that are more mobile (Masiello,
2004; Saiz et al., 2018; Santín et al., 2016). This fragmenta-
tion depends on the transformation of cell structures during
pyrolysis, and it is usually higher for grass than for wood
materials (Chrzazvez et al., 2014).

The combined effects of climate, vegetation, fire, catch-
ment topography and hydrology, soils, and PyC properties
will result in spatially variable post-fire redistribution of PyC
(Abney and Berhe, 2018; Berhe et al., 2018; Moody et al.,
2013). However, to which extent these drivers affect the mag-
nitude of post-fire PyC erosion and deposition still needs to
be elucidated (Abney and Berhe, 2018; Berhe et al., 2018;
Santín et al., 2016). It is difficult to assess the redistribu-
tion of PyC directly after a fire because substantial redistribu-
tion occurs during the first major rainfall event (Masiello and
Berhe, 2020). Rainfall simulation experiments allow con-
trollability and comparability between drivers, so that a di-
verse set of drivers can be repeatedly studied from a mech-
anistic point of view under the same conditions (Doetterl et
al., 2016; Rumpel et al., 2015). Furthermore, it is crucial to
study individual transport processes of PyC in closed systems
where PyC redistribution can be assessed fully with a single,
direct tracer method that allows for sufficient replication un-
der the same controlled conditions.

The objectives of this study were to assess the initial redis-
tribution of PyC during major rainfall events on soils through
splash and runoff as well as its vertical movement in the soil
column and how this depends on soil texture, slope angle and
PyC characteristics (feedstock and particle size). Therefore,
we conducted a simulated rainfall experiment on 0.25 m² soil
plots on which wood and grass PyC with a different isotopic
signal (δ¹³C) than the soils was applied. We estimated PyC
redistribution by collecting it in the runoff sediment, splashed
sediment, floating particles and soil cores and by measuring
the relative contribution of PyC to the δ¹³C signal of the sed-
iments, floating particles and soil cores. Specifically, we de-
termined (a) the effect of soil texture, slope angle and PyC
characteristics on the transport of PyC by surface runoff (i.e.,
overland flow); (b) the effect of soil texture, slope angle and
PyC characteristics on PyC redistribution by splash; (c) the
effect of soil texture, slope angle and PyC characteristics on
the washin of PyC into the soil; and (d) the effect of the ap-
plication of PyC on the redistribution of native soil organic
carbon (nSOC).

## 2 Material and methods

2.1 General approach

We used rainfall simulation experiments to study PyC erо-
sion and transport on soil plots. We used two forest soils
with different properties (Sect. 2.2 and Table 1) that had been
unburnt for at least 20 years and added wood or grass PyC
(Sect. 2.3 and Table 2) to the surface of the uppermost third
of the 0.25 m² plot. We used a multi-factorial experimen-
tal design that included two elements of four key drivers of
PyC relocation based on literature evidence. These included
soil texture (clayey loam (Cambisol) vs. sandy silt (Luvisol)),
slope angle (10° vs. 25°), PyC feedstock (wood PyC vs. grass
PyC) and PyC particle size (< 63 µm vs. 63 µm–2 mm). Each
of the two elements of the four drivers were combined and
assessed in triplicates (48 plots). In addition, for soil texture
and slope we also used four replicate control plots (16 plots)
where no PyC was added (hereafter labeled as “CT”). Dur-
ing each experimental run, rainfall was applied for 30 min to
one control plot and three plots where PyC was added. These
were randomly selected (total 16 runs). The applied rainfall
had an intensity of 102.8 mm h⁻¹ (51.4 ± 1.4 mm of applied
rainfall in total). After the rainfall simulation ended, we col-
lected the sediment that was transported by the runoff and
the sediment that was splashed to the sides and, also, took
soil cores to determine the redistribution of PyC across the
plots and the vertical transport of PyC in the soil. We used
the δ¹³C signal of the added PyC materials as a direct tracer
of PyC in this study to overcome methodological limitations
of other PyC detection methods.

## 2.2 Soils

We used the top 20 cm (without vegetation and litter) of two
Swiss forest soils that differ in soil texture, soil stability, SOC
content and soil hydrological properties (Table 1). The first
soil is a Cambisol (IUSS Working Group WRB, 2015), col-
lected from the Lägern site, next to the CarboEurope forest
flux site (CH-LAE, 47°28′42.0″ N, 8°21′51.8″ E), which is
a site of the Long-term Forest Ecosystem Research (LWF)
of the Swiss Federal Institute for Forest, Snow and Land-
scape Research (WSL). The site is located at 700 m a.s.l.
on the Lägern mountain, which belongs to the Swiss Jura
and is a mixed mountain forest dominated by beech, ash,
fir, lime and spruce (Ruehr et al., 2010). It has a clayey
loam texture, high aggregate stability (mean weight diame-
ter (MWD) = 1.74 ± 0.03) and SOC content of 3.6 ± 0.4 %
(Table 1). The second soil is a Haplic Luvisol that was col-
lected from the Möhlin site (Intercantonal Forest Observa-
tion Program in Switzerland). The Möhlin site is located on
an alluvial deposit close to the river Rhine (47°35′06.0″ N,
7°52′34.3″ E) at an elevation of 290 m a.s.l. and is domi-
nated by a woodruff beech forest stand (Braun et al., 2020).
The soil has a sandy silt texture, medium aggregate stabil-
<table><caption>**Table 1.** Total organic carbon (TOC), soil organic carbon stock (SOC), δ¹³C, bulk density, soil texture, pH, aggregate stability (mean weight diameter (MWD)), runoff ratio (runoff / rainfall), and soil water repellency of the Cambisol and Luvisol. Average values ± 1 standard error.</caption><thead><tr><th></th><th colspan="2">Cambisol</th><th colspan="2">Haplic Luvisol</th></tr></thead><tbody><tr><td>TOC [%]</td><td colspan="2">3.6 ± 0.4 (n = 72)</td><td colspan="2">2.24 ± 0.02 (n = 72)</td></tr><tr><td>SOC stock [Mg ha<sup>-1</sup>]<sup>1</sup></td><td colspan="2">36.0 ± 4.0 (n = 72)</td><td colspan="2">23.4 ± 0.2 (n = 72)</td></tr><tr><td>δ<sup>13</sup>C [%c]</td><td colspan="2">-29.07 ± 0.05 (n = 72)</td><td colspan="2">-29.87 ± 0.03 (n = 72)</td></tr><tr><td>Bulk density [g cm<sup>-3</sup>]</td><td>Before rainfall<br>0.94 ± 0.03 (n = 4)</td><td>After rainfall<br>1.01 ± 0.03 (n = 4)</td><td>Before rainfall<br>0.97 ± 0.01 (n = 4)</td><td>After rainfall<br>1.11 ± 0.03 (n = 4)</td></tr><tr><td>Texture [%]</td><td colspan="2">Clay loam<sup>2</sup><br>Sand: 45.5 ± 3.5<br>Silt: 24.2 ± 4.4<br>Clay: 31.5 ± 2.4</td><td colspan="2">Sandy silt<sup>3</sup><br>Sand: 40<br>Silt: 40<br>Clay: 20</td></tr><tr><td>pH [-]</td><td colspan="2">5.9 ± 0.5<sup>2</sup></td><td colspan="2">3.9<sup>3</sup></td></tr><tr><td>Aggregate stability [MWD]</td><td colspan="2">1.74 ± 0.03 (n = 6)</td><td colspan="2">0.89 ± 0.03 (n = 6)</td></tr><tr><td>Runoff ratio [%]<sup>4</sup><br>[Runoff (L) /rainfall (mm)]</td><td colspan="2">13.2 ± 0.8 (n = 32)<br>(1.7 ± 0.1/51.4 ± 1.4)</td><td colspan="2">88.5 ± 2.3 (n = 32)<br>(11.4 ± 0.3 / 51.4 ± 1.4)</td></tr><tr><td>Water repellency<sup>5</sup></td><td colspan="2">Very hydrophilic to hydrophilic (n = 5)</td><td colspan="2">Very hydrophilic (n = 5)</td></tr></tbody></table>

<table><caption>**Table 2.** Total C, δ¹³C and water repellency of wood PyC (derived from *Picea abies*) and grass PyC (derived from *Miscanthus sinensis*). Average values ± 1 standard error.</caption><thead><tr><th></th><th>Wood PyC<br>(Picea abies)</th><th>Grass PyC<br>(Miscanthus sinensis)</th></tr></thead><tbody><tr><td>Total C [%]</td><td>64.9 ± 1.3 (n = 5)</td><td>68.6 ± 1.8 (n = 5)</td></tr><tr><td>δ<sup>13</sup>C [%c]</td><td>-38.2 ± 0.2 (n = 5)</td><td>-13.8 ± 0.1 (n = 5)</td></tr><tr><td>Water repellency*</td><td>Extremely hydrophobic (n = 5)</td><td>Extremely hydrophobic (n = 5)</td></tr></tbody></table>

ity (MWD = 0.89 ± 0.03) and SOC content of 2.24 ± 0.02% (Table 1). In the following, the soils are named “Cambisol” and “Luvisol”, respectively. The collected soils were kept indoor under a protective foil and regularly rewetted with deionized water prior to the experiments. The soils were not sieved to < 2 mm due to the considerable amount of soil material (approximately 1 metric ton of each soil). Even though a soil that had been burned on the surface would have been more realistic, we used unburnt soils for practical reasons (large volume of soils, homogeneity of the surface, reproducibility of fire conditions, control of initial PyC amount).

## 2.3 Pyrogenic carbon (PyC) material: production and characterization

We used two types of PyC material (Table 2): PyC from spruce wood (*Picea abies*, hereafter called wood PyC and

labeled with “W”) grown under FACE conditions (Free Air Carbon Dioxide Enrichment; Hagedorn et al., 2003) and PyC from *Miscanthus* grass (*Miscanthus sinensis*), a C₄ plant (Hilber et al., 2012) (hereafter called grass PyC and labeled with “G”). The PyC was produced in several batches through pyrolysis, following the established method described in Hammes et al. (2006). Briefly, the biomass was loaded in a quartz tube (small chips of wood and grass of several centimeters in size), heated to 450 °C in a pyrolysis oven and charred for 4 h under a continuous N₂ stream, and collected after cooling. Pyrolysis has little effect on the δ¹³C of PyC (−38.0 ± 0.2‰ for spruce wood vs. −38.2 ± 0.2‰ for wood PyC, and −12.7 ± 0.1‰ for Miscanthus grass vs. −13.8 ± 0.1‰ for grass PyC). Mean mass recovery was 31.0 ± 0.5%, which is in line with yields reported by Keiluweit et al. (2010) for both grass and wood PyC at com-

<footnote n="1">¹ Calculated after M4 in Poeplau et al. (2017). ² Maestrini et al. (2014). ³ Braun et al. (2020). ⁴ Recorded runoff (L) was converted to runoff (m³). Runoff (m³) was divided by the soil plot area (0.25 m²) to calculate runoff depth (m). The runoff depth (mm) was then divided by the rainfall depth (mm) to calculate the runoff ratio (%). ⁵ According to the classification by Doerr (1998).</footnote>

<footnote>* According to classification by Doerr (1998).</footnote>
parable charring temperatures (400 to 500 °C). Afterwards, we homogenized the PyC of all batches by carefully mixing them in a bowl. To produce two sizes of PyC particles, we first passed the PyC through a 2 mm sieve and retained it on a 63 µm sieve to obtain the coarse particles (63 µm–2 mm, hereafter labeled with “CP”). Afterwards, a subsample was milled and passed through the 63 µm sieve (hereafter labeled with “FP”). Each of the two PyC particle size fractions was homogenized by mixing, and aliquots were sampled for characterization.

We determined PyC water repellency using the ethanol droplet test, as described in Doerr (1998). The wood and grass PyC were both extremely hydrophobic, with no detectable differences between them (Table 2). We characterized the PyC material by diffuse reflectance infrared Fourier-transformed spectroscopy (DRIFT) analysis (TENSOR 27 spectrophotometer, Bruker Fällanden, Switzerland). DRIFT spectra highlighted a higher aromaticity and condensation for the wood PyC, as indicated through higher absorption at $1730–1680 \text{ cm}^{-1}$ assigned to carbonyl / carboxyl C=O and at $1610–1570 \text{ cm}^{-1}$ assigned to aromatic C=C (Fig. S1). Cell structures were also better preserved for the wood PyC than the grass PyC, as indicated by a higher absorption for cellulose (C-O) at $1260–1210 \text{ cm}^{-1}$ (Chatterjee et al., 2012; Keiluweit et al., 2010).

## 2.4 Plot preparation

For the experiments, we used a soil plot ($0.5 \times 0.5 \times 0.2 \text{ m}$; $0.25 \text{ m}^2$ flume) and added clean Styrofoam (so that water can still drain) to the bottom 10 cm. We added the soil on top of the Styrofoam to reach a soil thickness of 10–12 cm and slightly compressed it to avoid any bagging of soil during experiments (bulk density between 0.9 (Cambisol) and $1.0 \text{ g cm}^{-3}$ (Luvisol)). We took particular care to also fill the edges of the plots and leveled the surface with a metal bar. We then applied the PyC material evenly on the surface of the uppermost third of the plot (upslope). The application rate was $118.7 \text{ g PyC m}^{-2}$ (equal of $77.0 \pm 1.5 \text{ g C}$ for wood PyC (total C = $64.9 \pm 1.3 \%$) and $81.4 \pm 2.1 \text{ g C}$ for grass PyC (total C = $68.6 \pm 1.8 \%$)) and we let it settle for at least 1 h to simulate surface deposition (Fig. 1). We choose this application rate based on literature estimates of standing biomass per square meter and PyC production and post-fire deposition (Proulx et al., 2015; Santín et al., 2015) and application rates ($106 \text{ g m}^{-2}$) used in field plot studies on PyC erosion (Rumpel et al., 2009).

The surface of the prepared plots were photographed with a high-end Sony Alpha 7R III & Zeiss Batis 18 mm fixed wide-angle lens (4K resolution with pixel-shift technology) attached to a tripod (fixed distance and angle to the floor) (Fig. 1b). Prior to rainfall simulation, the plots were adjusted to the respective slope angle (10° or 25°) and an overflow (metal plate) was added to the lowest sidewall and connected to a runoff channel and bucket (Fig. 1a). We monitored soil

moisture in each plot with a Decagon Em50 (inserted at 5 cm depth). Finally, we installed the splash shelter (corrugated panel) around each plot to ensure a closed system (Fig. 1a). We are aware that the setup used in our study will underestimate the splash erosion component. Splash erosion will not only occur to the sides of the soil plots (captured with the shelter around it), but also on the plots themselves. This latter component of splash erosion will be counted as either runoff erosion if the material leaves the plot in the direction of slope or distribution of soil, SOC and PyC within the soil surface and plot mid- and downslope. Since the processes of splash and runoff erosion are linked, we need to bear in mind that part of the eroded material by runoff may be attributable to splash erosion. Still, our results are the best estimation we could get for the two processes.

## 2.5 Rainfall simulation

We used the indoor, gravity-type rainfall simulator at the Swiss Federal Institute for Forest, Snow and Landscape Research (WSL) for the rainfall simulation experiments. The simulator includes drop-producing needles with an inner diameter of $0.05 \text{ mm}$ and a drop fall height of 7 to 8.5 m. The setup and general principles of the simulator have been described in detail in Berger et al. (2010), and basic data (i.e., water pressure, flow, temperature, rainfall characteristics) can be found in the Supplement (Table S1 and Fig. S2). The simulator setup produced raindrops that reached terminal velocities and drop size distribution (determined using the oil method; Kathiravelu et al., 2016; data not shown) close to natural rainfalls (Abd Elbasit et al., 2010; Abudi et al., 2012; Aksoy et al., 2012). We used only one simulator element ($1.05 \times 3.25 \text{ m}$) and a designated area of $0.8 \times 2.8 \text{ m}$ under the simulator for the experiments. This allowed us to place four of the $0.25 \text{ m}^2$ plots side by side below the simulator and apply rainfall to them simultaneously. The rainfall intensity in the simulation area was measured three times using 56 small ($8.5 \text{ cm}$ diameter) funnel gauges (Fig. S2). The simulator produced constant rainfall of $102.8 \text{ mm h}^{-1}$ ($51.4 \pm 1.4 \text{ mm}$ in 30 min). The Christiansen uniformity coefficient of 84% indicates a uniform distribution of the rainfall over the simulation area (Aksoy et al., 2012; Christiansen, 1942; Lassu and Seeger, 2015).

Because we applied rainfall to four plots at a time, we prioritized homogeneous distribution of rainfall over the simulated area to ensure controlled and comparable conditions between the plots. The uniformity of the rainfall over the simulation area decreased rapidly with intensities smaller than $100 \text{ mm h}^{-1}$, and therefore this intensity was chosen. The simulated rainfall depth of 51.4 mm for 30 min represents a rainfall event with a return interval of 51–206 years for three long-term meteorological stations near the Lägern site (Zurich Kloten: 206 (95% confidence interval: 51 to > 300), Zurich Affoltern: 69 (21 to > 300) and Zurich Fluntern: 93 (25.5 to > 300)). For the stations in close proximity to the
Experimental setup

<figure><img src="image_4.png" /><figcaption>(a)</figcaption></figure>

PyC surface dynamics

<figure><img src="image_5.png" /><figcaption>(b)</figcaption></figure>

**Figure 1.** Experimental setup, including the rainfall simulator and an example of a 0.25 m² soil plot (a) and visual assessment of the surface of the Cambisol and Luvisol (25° slope and with coarse wood PyC) (b). Each 0.25 m² soil plot was photographed before and after the 30 min rainfall simulation experiment. Visual assessment showed vertical movement of PyC in the Cambisol (white arrow in b) and surface redistribution of PyC on the Luvisol (black circles in b).

Möhlin site, it represents an event with a return interval of 99–117 years (Rünenberg: 98.5 (25 to > 300) and Basel: 116.5 (28 to > 300); 1982–2018 data, Federal Office of Meteorology and Climatology MeteoSwiss, 2019).

## 2.6 Sampling, sample preparation and analysis

After the rainfall simulation experiment, we flushed the runoff channel with a known volume of deionized water and recorded the total weight of the bucket that already contained the surface runoff and the eroded material. To collect splash sediment, we washed the splash panel with a known volume of deionized water and collected it in the splash basin that already contained the eroded splash material. We transferred all the collected splash material to a bucket and weighed it. The buckets with the runoff and splashed material were set aside for sedimentation for > 24 h before carefully collecting the particles floating on the water surface, pumping out the water with a bell jar attached to a peristaltic pump and finally collecting the sediment that settled at the bottom of the buckets. The sediment and floating particles of both the runoff

and the splashed material were separately dried at 40 °C and weighed. Finally, sediment samples of both the runoff and splash were milled. The floating particles of both the runoff and splash were milled in a mortar by hand because of the small amount of material. The collected sediment and floating particles were analyzed for total organic carbon (TOC; representing nSOC for control plots and nSOC + PyC for plots where PyC was applied) and δ¹³C, relative to the international Vienna Pee Dee Belemnite (VPDB) standard, using cavity ring-down spectroscopy with a dry combustion system (CRDS Picarro, Inc. 2020).

Prior to sampling the soil after the experiment, each plot was photographed as described previously (i.e., similar to before the rainfall simulation). We sampled the soil with a soil corer (steel cylinder with 5 cm diameter and 10 cm length). We took cores at three random locations in the three slope positions (upslope, midslope, downslope), cut the cores into three depth increments (0–1, 1–3 and 3–10 cm) and homogenized the material from the three cores per depth to obtain one composite sample per slope position, depth and plot. Soil samples were air-dried, sieved to < 2 mm and milled. The
soil samples were analyzed similarly as the collected sediment and floating particles for TOC and δ¹³C. Additionally, we took cores from control plots for each soil before and after rainfall simulation and analyzed them for the bulk density. We also tested the aggregate stability (mean weight diameter (MWD) calculation) of the soils with the fast wetting method described in Le Bissonnais (2016). Using the same method as for PyC materials, we tested soil water repellence according to the ethanol droplet test of Doerr (1998).

## 2.7 Quantification of the PyC contribution to TOC using δ¹³C and C recovery

To determine PyC redistribution during a rainfall event, we used the differences in δ¹³C of the forest soils (−29.1 ± 0.1‰ for the Cambisol and −29.9 ± 0.1‰ for the Luvisol) and the PyC materials (−38.2 ± 0.2‰ for the wood PyC and −13.8 ± 0.1‰ for the grass PyC). The δ¹³C difference of 8.3‰–16.1‰ between the soils and PyC materials was much larger than the maximal drift of the CRDS analyzer (−0.5‰) and allowed us to differentiate between nSOC and PyC in the TOC. We used a two-pool isotope-mixing model to calculate the contribution of the added PyC to the δ¹³C signal of a sample (sediment, floating particles or soil cores) using Eq. (1):

$$f = 1 - \left( \frac{(\delta^{13}C_{\text{sample}} - \delta^{13}C_{\text{PyC_app}})}{(\delta^{13}C_{\text{control}} - \delta^{13}C_{\text{PyC_app}})} \right) \times 100, \quad (1)$$

where f is the fraction of OC derived from the PyC (or PyC fraction, %), δ¹³Csample is the δ¹³C value of the sample, δ¹³CPyC_app is the average δ¹³C value of the added PyC (Table 2) and δ¹³Ccontrol is the average δ¹³C value of the control plots for the runoff, splashed sediments, runoff and splash floating particles (representing the nSOC of the TOC). The PyC fraction (%) was subsequently multiplied with the TOC (nSOC + PyC, g), and finally the quantity of PyC (g C) was divided by the amount of added PyC (g C) to calculate PyC recovery (% of total added PyC). For the soil core calculations (Fig. 6 and Table S2), we used the average δ¹³C value of all control samples (Table 1) to ensure a stable background signal to calculate the PyC fraction. For the soil core samples, we could not convert the PyC fraction to a reliable PyC recovery value because both the soil mass and the TOC contents of the soil core samples were too variable.

## 2.8 Statistical analyses

We ran Levene's test to check the homogeneity of variance assumption (center is equal to the mean). We ran a two-way ANOVA model for the full dataset on eroded soil mass, eroded TOC, PyC recovery (runoff and splash sediment, runoff and splash floating particles) and subsequently a two-way ANOVA model per soil type (Cambisol and Luvisol) for the same datasets. For the soil core data, we used a two-way ANOVA model for each slope position (upslope,

midslope and downslope) and depth increment (0–1, 1–3, 3–10 cm) for the full dataset and subsequently for the individual soil types. We used the Shapiro–Wilk tests on the ANOVA residuals to check the normality assumption and Fisher's least significant difference (LSD) post-hoc tests (alpha = 0.05, p. adj = Bonferroni) on the two elements of the four drivers. For changes in nSOC export after application of PyC compared to corresponding controls, we used a Welch two-sample t-test (95 % confidence interval). All statistical analyses were completed using the R packages “agricolae” and “car” in RStudio Version 3.5.2 (R Core Team, 2018).

# 3 Results

## 3.1 Redistribution of soil and total organic carbon (TOC)

### 3.1.1 Amount of runoff and relocated quantities of soil and floating particles

The amount of surface runoff generated was much less for the Cambisol than the Luvisol plots, with average runoff ratios for all plots of 13.2 ± 0.8 % and 88.5 ± 2.3 %, respectively (Table 1). Soil moisture was higher in the Cambisol and for both soils for the 10° plots than the 25° plots (Fig. S3). For the Cambisol, initial soil moisture increased rapidly over the first 5 min and then steadily increased until the end of the rainfall simulation for both slope angles. For the Luvisol, soil moisture increased rapidly but less pronouncedly during the first 10 min and remained stable after 15 min for the 10° slope plots and after around 20 min for the 25° plots. The relatively low moisture contents of both soils at the end of the experiment and the flattening of the moisture curves towards the end of the simulation indicate that the soils were not fully saturated, and infiltration rates dropped due to surface sealing, especially for the Luvisol (Fig. S3). This was also visually observed during experiments.

The amount of soil that was transported by the runoff (i.e., the soil mass for control plots and soil + PyC mass for plots where PyC was applied) was significantly different for the two soil types: on average 1.3 ± 0.2 g (= 5.2 ± 0.8 g m²) for the Cambisol and 196.7 ± 14.3 g (= 786.8 ± 57.2 g m²) for the Luvisol (p < 0.001; Fig. 2a). Note that because PyC represented < 2 % of total mass, its influence on the total mass of transported soil could be neglected for this calculation. The runoff-driven erosion rates varied between 2.8 ± 0.3 g m⁻² (Cambisol under 10° slope) and 1156.8 ± 160.8 g m⁻² (Luvisol under 25° slope) for the 30 min rainfall simulation. The sediment transport was about 2 times higher for plots under steeper slopes (average for all 10° plots: 70.4 ± 13.6 g and all 25° plots: 127.6 ± 24.2 g). The effect of slope was significant for the Cambisol (p = 0.03) and Luvisol (p < 0.001).

Soil type was also the main explanatory variable for the average amount of soil eroded by splash (Fig. 2b). It
<figure><img src="image_6.png" /><figcaption>**Figure 2.** Amount of sediment (g) transported by the runoff (a) and splash (b) as well as floating particles transported by runoff (c) and splash (d) for each treatment after 30 min of rainfall (total: 51.4 ± 1.4 mm) (CT: control plots; G: grass PyC; W: wood PyC; 25: 25° slope; 10: 10° slope; FP: fine PyC (< 63 µm); CP: coarse PyC (63 µm to 2 mm)). Values are given as means (±1 standard error) and correspond to the mass of soil for control plots (CT: *n* = 4) and mass of soil + PyC for plots where PyC was applied (*n* = 3; PyC only represented < 2% of total mass).</figcaption></figure>

was 31% less (*p* < 0.001) for the Cambisol (65.5 ± 3.6 g (=262.0 ± 14.4 g m⁻²)) than the Luvisol (95.5 ± 4.5 g (=382.0 ± 18.0 g m⁻²)). Transport rates by splash ranged between 178.8 ± 16.0 g m⁻² (Cambisol under 10° slope) and 468.4 ± 73.6 g m⁻² (Luvisol under 25° slope) for the 30 min rainfall simulation.

The total transport of floating particles (i.e., native SOC (nSOC) for control plots and nSOC + PyC for plots where PyC was applied) by runoff was different between soil types. It was 0.03 ± 0.01 g for the Cambisol and 0.49 ± 0.09 g for the Luvisol (*p* < 0.001). For PyC particle sizes, it was 0.6 ± 0.1 g when PyC was applied as coarse particles (CP), 0.09 ± 0.02 g for fine particles (FP) and 0.08 ± 0.02 g for controls (CT, no PyC applied) (*p* < 0.001; Fig. 2c). The mass of floating particles eroded by splash was larger than for the runoff and also dependent on soil type (Cambisol: 0.17 ± 0.05 g and Luvisol: 1.0 ± 0.2 g, *p* < 0.001). It was further also dependent on PyC particle size (CP: 1.4 ± 0.3 g, FP: 0.14 ± 0.02 g and CT: 0.10 ± 0.02 g, *p* < 0.001; Fig. 2d). However, the total mass of floating particles transported by runoff or splash was only significantly higher with the application of coarse PyC to the Luvisol (significant interaction

of the drivers “soil type × PyC particle size” in the ANOVA model: *p* < 0.001).

### 3.1.2 Transported TOC

Similar to the mass of soil that was transported, the amount of TOC transported by runoff (i.e., native SOC (nSOC) for control plots and nSOC + PyC for plots where PyC was added) was almost negligible for the Cambisol but notable for the Luvisol (0.08 ± 0.01 g C and 7.3 ± 0.5 g C, respectively, *p* < 0.001, Fig. 3a). Steeper slope angles (25°) resulted in 144% more TOC transport by the runoff but did not change the proportions of eroded TOC/soil. This effect holds true for both soil types (Cambisol (*p* = 0.03) and Luvisol (*p* = 0.0005)). The strong interaction of soil type and slope in our model suggests that more TOC was transported by runoff on steeper slopes on the Luvisol in absolute terms (*p* = 0.0003; Fig. 3a). Transport rates of TOC by runoff ranged between 0.08 ± 0.04 g C m⁻² (Cambisol under 10° slope) and 44.0 ± 5.6 g C m⁻² (Luvisol under 25° slope) for the 30 min rainfall simulation. We found higher export of TOC (nSOC + PyC) by runoff when fine PyC particles (FP) were applied but not when coarse PyC particles
<figure><img src="image_7.png" /><figcaption>**Figure 3.** Amount of TOC (g) transported by runoff (a) and splash sediment (b) as well as the floating particles in runoff (c) and splash (d) for each treatment after 30 min of rainfall (total: 51.4 ± 1.4 mm) (CT: control plots; G: grass PyC; W: wood PyC; 25: 25° slope; 10: 10° slope; FP: fine PyC (< 63 µm); CP: coarse PyC (63 µm to 2 mm)). Values are given as means (±1 standard error), and the TOC values represent native SOC (nSOC) for control plots (CT: *n* = 4) and nSOC + PyC for plots where PyC was applied (*n* = 3).</figcaption></figure>

(CP) were applied, compared to control plots (CT). However, we identified this only for the Luvisol (FP: 9.1 ± 0.8 g C, CP: 6.5 ± 0.5 g C and CT (no PyC applied): 5.8 ± 0.7 g C; *p* = 0.0009), indicating that fine PyC particles preferentially contributed to the transported TOC by runoff on the Luvisol (soil type × PyC particle size: *p* = 0.003; Fig. 3a).

Splash erosion of TOC was slightly higher for the Luvisol (Cambisol: 2.9 ± 0.2 g C and Luvisol: 3.3 ± 0.2 g C, *p* = 0.05; Fig. 3b). All plots of both soils receiving PyC showed higher splash erosion of TOC irrespective of PyC feedstock or particle size compared to control plots, but we found no difference between either wood and grass PyC or fine and coarse PyC for any of the soils (Fig. 3b). Transport rates of TOC through splash ranged between 6.8 ± 0.8 g C m⁻² (Cambisol under 10° slope) and 16.4 ± 2.8 g C m⁻² (Luvisol under 25° slope) for the 30 min rainfall simulation.

The transported quantities of TOC (i.e., nSOC for control plots and nSOC + PyC for plots where PyC was applied) in the floating particles for both the runoff and splash differed between the soil types and PyC particle sizes (Fig. 3c–d). The mass of relocated TOC by runoff of floating particles was 0.011 ± 0.002 g C for the Cambisol and 0.24 ± 0.04 g C for the Luvisol (*p* < 0.001; Fig. 3c). Application of both

wood and grass PyC as coarse particles resulted in more transport of TOC in floating particles by runoff compared to the control plots, but this was not the case for the fine PyC particles. The particle size was significant for the Luvisol, but not the Cambisol, which suggests that the coarse PyC contributed to the transported TOC of floating particles in the runoff for the Luvisol (soil type × PyC particle size: *p* < 0.001; Fig. 3c). The mass of TOC in floating particles relocated by splash erosion was 0.06 ± 0.01 g C for the Cambisol and 0.6 ± 0.1 g C for the Luvisol (*p* < 0.001; Fig. 3d). For both soils, application of wood and grass PyC as coarse particles resulted in more relocation of TOC in floating particles by splash compared to the controls, and again this was not the case for the fine PyC particles (*p* < 0.001; Fig. 3d).

## 3.2 Redistribution of PyC by runoff and splash: recovery of added PyC

We observed similar trends for the redistribution of the added PyC as for the transported soil and TOC (Figs. 2–3), including clear differences between the two soil types (Fig. 7). PyC relocation (as a percentage of total added PyC) through runoff and splash erosion combined, for both sediment and floating particles, varied between 10.5 ± 1.4% for the Cam-
<figure><img src="image_8.png" /><figcaption>**Figure 4.** PyC recovery (% of total added PyC) in sediment transported by runoff (a) or splash (b), and floating particles transported by runoff (c) and splash (d) for each treatment after 30 min of rainfall (total: 51.4 ± 1.4 mm) (G: grass PyC; W: wood PyC; 25: 25° slope; 10: 10° slope; FP: fine PyC (*<* 63 µm); CP: coarse PyC (63 µm to 2 mm)). Average values ± 1 standard error (n = 3).</figcaption></figure>

bisol and 61.3 ± 3.4% for the Luvisol (p < 0.001; Figs. 4 and 7). Moreover, we recovered much more of the added PyC in the sediments and floating particles transported by runoff and splash combined after application of wood than grass PyC (W: 43.4 ± 6.6% and G: 28.4 ± 4.6%, p < 0.001; Fig. 4).

PyC in the runoff sediment (% of total added PyC) was approximately 300 times more for the Luvisol (32.4 ± 3.8%) than the Cambisol (0.09 ± 0.02%, p < 0.001; Fig. 4a). Application of wood PyC resulted in more PyC relocation in sediment by runoff (19.4 ± 5.0%) compared to grass PyC (13.1 ± 3.3%), and this effect was significant for both soils (Cambisol: p = 0.04 and Luvisol: p = 0.009). Application of fine PyC (23.1 ± 5.3%) resulted in more PyC redistribution of the sediment by runoff compared to coarse PyC particles (9.4 ± 2.2%) in the full ANOVA model, but the effect differed for the two soils (Fig. 4a). There was more PyC relocation for coarse particles for the Cambisol (p = 0.01; less than < 0.13 ± 0.03% for both particle sizes), but, for the Luvisol, there was more PyC relocation for the fine particles (FP: 46.1 ± 4.6% and CP: 18.7 ± 2.0%, p < 0.001). In contrast to the amount of transported soil and TOC by the runoff (Figs. 2a and 3a), slope angle did not affect PyC redistribution (p = 0.09; Fig. 4a).

In accordance with the larger mass of splashed soil (Fig. 2b), we found greater PyC relocation (% of total added PyC) by splash for the Luvisol (15.2 ± 1.4%) than the Cambisol (9.5 ± 1.5%, p = 0.0006; Fig. 4b). When averaged for the two soils, redistribution of PyC by splash was twice as much when wood PyC (16.0 ± 1.7%) was applied compared to grass PyC (8.6 ± 1.0%, p < 0.001). Relocation of PyC by splash was greater when fine PyC particles were applied compared to coarser ones (FP: 14.3 ± 1.6% and CP: 10.3 ± 1.5%), but this effect was only significant for the Cambisol (soil type × PyC particle size: p < 0.0003; Fig. 4b).

Redistributed quantities of PyC as floating particles were significantly different for the two soil types and PyC particle sizes (Fig. 4c–d). Relocated PyC in floating particles in the runoff was 0.07 ± 0.03% of initially added PyC for the Cambisol and 3.6 ± 0.8% for the Luvisol (p < 0.001; Fig. 4c). Application of coarse PyC particles resulted in significantly higher relocation of PyC in floating particles in runoff compared to finer PyC (CP: 3.6 ± 0.8% and FP: 0.02 ± 0.01%; Cambisol (p = 0.001) and Luvisol (p < 0.001); Fig. 4c). Relocated PyC in floating particles of splash accounted for 0.8 ± 0.2% (Cambisol) and 10.1 ± 2.3% (Luvisol) of the recovered PyC (p < 0.001; Fig. 4d). The amount of relo-
<figure><img src="image_9.png" /><figcaption>**Figure 5.** Differences in native SOC export (Δ nSOC to control in grams) between the PyC treatments (nSOC = TOC – PyC) and the corresponding controls (nSOC = TOC) in sediment transported by runoff (a), splash (b) and floating particles in runoff (c) and splash (d) after 30 min of rainfall (total 51.4 ± 1.4 mm) (G: grass PyC; W: wood PyC; 25: 25° slope; 10: 10° slope; FP: fine PyC (< 63 µm); CP: coarse PyC (63 µm to 2 mm)). Average values ± 1 standard error (n = 3). Significant changes at *p* < 0.05 are marked with an asterisk (*).</figcaption></figure>

cated PyC in floating particles by splash was higher for coarser particles than finer ones (CP: 10.9 ± 2.2% and FP: 0.03 ± 0.01%), and this effect was significant for the Cambisol (p = 0.0003) and Luvisol (p < 0.001; Fig. 4d).

**3.3 Changes of nSOC dynamics after application of PyC**

Our $\delta^{13}$C approach (using $^{13}$C-labeled PyC material) and the mass balance of TOC and PyC allowed us to estimate the effect of PyC application on the transport of native SOC (nSOC). We compared the transport of nSOC for control plots (nSOC = TOC) with plots where we added PyC (nSOC = TOC – PyC). Changes in nSOC export through runoff after application of PyC were negligible for the Cambisol ($< 0.5 \pm 0.1 \text{ g C m}^{-2}$) but important for the Luvisol (Fig. 5a). For the Luvisol, the changes varied from reduced export of the order of $8.4 \pm 5.2 \text{ g C m}^{-2}$ (fine-grained wood PyC on 25° slope; $p = 0.25$) to higher export of the order of $8.4 \pm 4.0 \text{ g C m}^{-2}$ (fine-grained grass PyC on 10° slope; $p = 0.16$) compared to controls (Fig. 5a). Changes of nSOC export through splash after application of PyC were important for the Cambisol at the 10° slope but small for the Luvisol (Fig. 5b). For the 10° Cambisol plots, we observed a higher export of nSOC after PyC application than

for the control plots in the range of $3.6 \pm 1.6 \text{ g C m}^{-2}$ (fine-grained grass PyC; $p = 0.13$) to $5.2 \pm 0.4 \text{ g C m}^{-2}$ (fine-grained wood PyC). For the wood PyC application, higher exports were significant for fine ($p = 0.01$) and coarse PyC particles ($p = 0.002$). Changes in nSOC export as floating particles through runoff and splash after PyC application were small and highly variable (Fig. 5c–d).

**3.4 Distribution of PyC on the soil surface and in the soil**

**3.4.1 Upslope position**

For the upslope position (i.e., uppermost third where PyC was initially added), the distribution of PyC on the soil surface and in the soil after the rainfall simulation differed strongly for the two soil types (here reported as the fraction of OC derived from the PyC in percent (or PyC fraction)). We found more PyC at all three depths (0–1, 1–3 and 3–10 cm) in the Cambisol than the Luvisol (Fig. 6a–b and Table S2). For the surface layer (0–1 cm), the PyC fraction was $11.4 \pm 1.6\%$ for the Cambisol and $7.5 \pm 0.9\%$ for the Luvisol ($p = 0.0009$). At 1–3 cm depth, it was $4.8 \pm 0.5\%$ for the Cambisol and $0.5 \pm 0.2\%$ for the Luvisol ($p < 0.001$). At 3–10 cm depth, the difference was $2.0 \pm 0.3\%$ for the Cam-
<figure><img src="image_10.png" /><figcaption>**Figure 6.** Distribution of PyC (PyC fraction is the fraction of OC derived from the PyC in percent) in soil cores for the Cambisol (a, c, e) and Luvisol (b, d, f) along the 0.25 m² plot (upslope: a–b; midslope; c–d and downslope: e–f) and with depth (0–1, 1–3, 3–10 cm) for each treatment after 30 min rainfall (total: 51.4 ± 1.4 mm) (G: grass PyC; W: wood PyC; 25: 25° slope; 10: 10° slope; FP: fine PyC (< 63 µm); CP: coarse PyC (63 µm to 2 mm)). Average values ± 1 standard error (n = 3).</figcaption></figure>

bisol and 0.8 ± 0.2% for the Luvisol (p = 0.007). The visual assessment of the soil surface and vertical profile confirmed that more PyC remained on the surface or was washed in for the Cambisol than the Luvisol (Fig. 1b).

In addition to soil type, the distribution of PyC on the soil surface (0–1 cm) of the upper slope depended on PyC feedstock (Fig. 6a–b and Table S2). A larger PyC fraction remained on the surface when wood PyC (11.5 ± 1.5%) was applied than when grass PyC (7.4 ± 1.0%) was applied, and this effect was significant for the Cambisol (p = 0.005) and Luvisol (p = 0.03). Furthermore, significantly more PyC remained on the surface of the Cambisol when coarser PyC particles (18.1 ± 1.5%) were applied than finer ones (4.6 ± 0.7%; p < 0.001). The strong interaction of soil type and PyC particle size in our model suggests that coarse PyC remained on the soil surface of the Cambisol in the upslope position (p < 0.001; Fig. 6a and Table S2).

### 3.4.2 Mid- and downslope

In the midslope position, significant differences were only found for the Luvisol and were mainly related to PyC feedstock (Fig. 6c–d and Table S2). There was more PyC fraction on the surface (0–1 cm) of the Luvisol when

wood PyC (5.0 ± 0.9%) was applied than for grass PyC (1.6 ± 0.3%; p = 0.002). This was also the case at 1–3 cm depth (1.2 ± 0.5% for wood PyC compared to 0.3 ± 0.2% for grass PyC; p = 0.02). In addition, there was significantly more PyC at 1–3 cm depth in the midslope position for the Cambisol than the Luvisol (PyC fraction: 1.9 ± 0.4% for the Cambisol and 0.7 ± 0.3% for the Luvisol; p = 0.002). This difference was also seen for the downslope cores (Cambisol: 1.9 ± 0.5% and Luvisol: 0.9 ± 0.3%) but was not significant (p = 0.11). The PyC fraction on the soil surface (0–1 cm) at the mid- and downslope positions was higher for the Luvisol than the Cambisol (Figs. 6c–f and 1b): 2.3 ± 0.5% for the Cambisol and 3.3 ± 0.6% for the Luvisol at the midslope position (p = 0.14). Downslope, it was 1.1 ± 0.4% for the Cambisol and 2.3 ± 0.5% for the Luvisol (p = 0.058).

## 4 Discussion

### 4.1 PyC redistribution by rainfall

Our study provides evidence for a quick redistribution of PyC by intense rainfall. Between 0.18 ± 0.05% and 36.0 ± 4.6% of the initially added PyC was transported by runoff (both as sediment and floating particles), and between 10.3 ± 1.7%
and 25.3 ± 3.7% of the initially added PyC was transported as splash (both as sediment and floating particles) during 30 min rainfall events (51.4 mm) on 0.25 m² plots (Figs. 4 and 7). Therefore, our data confirm that the fate and mobility of PyC on short timescales depends to a great extent on its initial interaction with water (Masiello and Berhe, 2020). The portions of PyC relocated by runoff (% of total added PyC; Fig. 4a and c) are of the same order of magnitude as observed for post-fire, plot-scale erosion field studies. Rumpel et al. (2009) reported that between 7% and 29% of initially applied PyC was transported by runoff. Cotrufo et al. (2016) found that 11% of PyC present in the organic layer was exported during the first year after a fire, and Major et al. (2010) estimated that around 20% to 53% of applied PyC must be relocated by erosion. In addition, Rumpel et al. (2009) reported PyC erosion by splash of 31.2 ± 21.3%, and our values of PyC recovery are well within this range (Fig. 4b and d). However, it has to be mentioned that other studies have also reported limited transport of PyC (< 2% of TOC in runoff) after 62 years after a fire (Güereña et al., 2015).

Initial rainfall determines not only the redistribution of PyC on the surface, but also the quantity of PyC that moves into the soil (Masiello and Berhe, 2020). We recovered part of the initially added PyC (PyC fraction) at 1–3 and 3–10 cm depth at the upslope position where it was initially applied, especially for the Cambisol (6.8% (Cambisol) and 1.3% (Luvisol); Fig. 6a–b). This shows that PyC moved through the soil profile within 30 min under unsaturated conditions. Due to the small amounts of PyC compared to the total mass of soil in our plots (on average 26.0 ± 0.2 kg soil per plot), we could only calculate the fraction of OC that is PyC (PyC fraction) in the soil column, but no PyC recovery (% of total added PyC). This limits the comparison with literature values. We chose larger quantities of soil (larger plot size) to eliminate possible boundary effects of the plots on PyC redistribution. However, in accordance with our findings, vertical movement of ¹³C-labeled wood PyC (3% to 4% of applied PyC) up to 10–15 cm depth in soil cylinders after 10 months under field conditions has been reported for one of the sites from which we took the soil for our plots (Cambisol at the Lägern site) (Singh et al., 2014). In other studies conducted on soil plots or soil microcosms (between 8 and 20 cm long and 10 cm in diameter) in the field or in the laboratory, relocated quantities by vertical movement up to 10 cm depth after 1–2 years varied between < 1% and 2.3% of initially applied PyC (in particulate or dissolved form) (Hilscher and Knicker, 2011; Maestrini et al., 2014; Major et al., 2010). Even larger amounts (23% to 46% of initially applied PyC) have been reported for plot-scale rainfall simulations in the tropics, but this vertical transport was limited to 1 cm depth (Rumpel et al., 2009).

## 4.2 Effect of PyC application on nSOC redistribution

By using ¹³C-labeled PyC, we were able to show for the first time (to our knowledge) that the application of PyC to the soil surface and its subsequent redistribution affect the fate and redistribution of native SOC (nSOC). The changes in nSOC export by runoff and splash after application of PyC were of the same order of magnitude as the PyC flux after the rainfall event but highly variable, and the underlying processes are not fully clear and need further investigation (Fig. 5). These changes could be related to the sorption and stabilization of nSOC to PyC surfaces (Jiang et al., 2019; Singh et al., 2014), or the strong affinity of PyC to sorb to mineral surfaces, which can promote the mobilization of less effectively adsorbed nSOC through desorption (Jiang et al., 2016). However, it seems unlikely that these processes take place within minutes. Another possible explanation could be that PyC particles on the soil surface increase the soil hydrophobicity and lead to a longer contact time between water and nSOC, which may promote its export. However, it is still surprising that such a process would result in such a large export flux of nSOC. More specific experiments are needed to fully understand these processes.

## 4.3 Key drivers of soil, TOC and PyC redistribution

### 4.3.1 Soil type

Soil type was the main explanatory variable that influenced soil, TOC and PyC redistribution by surface runoff (Figs. 2a, 3a and 4a). This can be related to the soils' physical and hydrological properties. The higher runoff (7 times higher for the Luvisol than the Cambisol; Table 1) and reduced infiltration rates (Fig. S3) for the Luvisol, despite its sandy silty texture, can be explained by its lower aggregate stability (Table 1). Runoff ratios between 13.2 ± 0.8% (Cambisol) and 88.5 ± 2.3% (Luvisol) for a 102.8 mm h⁻¹ rainfall on 0.25 m² plots are comparable to those reported from rainfall simulation experiments (80–85 mm h⁻¹ rainfall on 0.28 m² plots) in Portugal, with runoff coefficients of 7% to 55% on Leptosols and Umbrisols (Malvar et al., 2013). Difference in runoff amount for the two soil types was only by a factor of 7 but the erosion differed by a factor of 150 (Fig. 2a), which indicates that the higher erosion on the Luvisol is a result of the Luvisols' physical instability and susceptibility to erosion (i.e., the low aggregate stability and SOC content) and not only a result of the higher water flow (Koiter et al., 2017). Surface sealing is generally stronger for soils with a coarser soil texture and lower organic matter content (Armenise et al., 2018). In contrast, clay-rich soils with a high physical stability (i.e., high aggregate stability) and higher TOC content are less prone to erosion, as they do not lead to rapid surface sealing and therefore slow down runoff generation and erosion (Berhe and Kleber, 2013; de Nijs and Cammeraat, 2020; Thomaz, 2018). The eroded quan-
tities of soil (5.2 ± 0.8 g m⁻²) and TOC (0.32 ± 0.04 g C m⁻²) for the Cambisol are in the same range as for a clay-rich Alfisol (28 ± 76 to 60 ± 249 g m⁻²) and TOC (0.9 ± 9.8 to 2.2 ± 16.2 g C m⁻²) on 1 m² field plots (Chaplot et al., 2005). For the Luvisol, eroded quantities of soil (786.8 ± 57.2 g m⁻²) and TOC (29.2 ± 2.0 g C m⁻²) are of the same order of magnitude as for a field study conducted on loess-derived Luvisols in Belgium (using 45 mm h⁻¹ on 0.72 m² plots), with a soil loss of 330.2 ± 525.6 g m⁻² h⁻¹ and a SOC loss of 4.8 ± 5.5 g C m⁻² h⁻¹ (Wang et al., 2010). Also Schindler Wildhaber et al. (2012) found clear differences in soil losses by runoff: 894 ± 282 g m⁻² for a silty soil with low SOC content (1.7 ± 0.9 % OC) compared to 191 ± 54 g m⁻² for a clay-rich soil with high SOC content (5.2 ± 2.3 % OC) under 60 mm h⁻¹ for 2 h in field and laboratory studies. They related the differences in the losses to variable soil structural stabilities and therefore susceptibility to erosion. The higher values of soil and SOC relocation in our study could partially be explained by the higher rainfall intensity (102.8 mm h⁻¹) since soil erosion is significantly correlated to rainfall intensity (Chaplot and Le Bissonnais, 2003).

Soil type is also a main explanatory variable for PyC relocation by runoff (Figs. 4a and 7). The higher redistribution of PyC on the Luvisol than the Cambisol can be explained by the same processes as soil and TOC transport (i.e., rapid surface sealing, higher erodibility and higher runoff ratio (and thus higher sediment transport) for the Luvisol than for the Cambisol). The high runoff and transport rates on the Luvisol promoted the redistribution of the low-density PyC particles on the soil surface (Abney and Berhe, 2018; Bird et al., 2015; Rumpel et al., 2006). Surface sealing can be increased when aggregates are broken down and PyC (ash and char) is washed into the soil and fills flow pathways in mechanically weaker soils (Certini, 2005; Onda et al., 2008). In contrast, the physical and hydrological properties of the Cambisol changed very little during the rain event, i.e., only 5.2 ± 0.8 g sediment per square meter was recovered after 30 min (indicating reduced aggregate breakdown and soil loss), and soil moisture was still increasing at the end of the rainfall simulation (indicating continuous infiltration (Fig. S3)). This caused the 7 times lower runoff and 300 times smaller PyC relocation by runoff on the Cambisol than the Luvisol.

Redistribution of soil, TOC and PyC by splash was higher for the Luvisol, but differences with the Cambisol were much smaller than for the transport of soil, TOC and PyC by the runoff (Figs. 2b, 3b and 4b). The measured quantities of eroded soil by splash (262.0 ± 14.4 g m⁻² (Cambisol) and 382.0 ± 18.0 g m⁻² (Luvisol)) are in agreement with reported values of splashed soil for a clay loam (290 ± 10 g m⁻²) and for a silt loam (550 ± 10 g m⁻²) or sand (730 ± 20 g m⁻²) under 30 mm h⁻¹ rainfall (Legout et al., 2005). Splash erosion, or the impact of raindrops on soil particles, is often considered the first and dominant process of soil detachment and transport over small distances and depends on rainfall characteristics and soil surface properties (Malam Issa et al., 2006; de Nijs and Cammeraat, 2020).

The amount of splashed soil by raindrops generally increases with decreasing physical stability of soil (i.e., faster aggregate breakdown) and can therefore explain the larger amounts of splashed sediment for the Luvisol than the Cambisol in our study (see Legout et al., 2005). However, the measured quantities of eroded TOC by splash for the Cambisol (11.6 ± 0.8 g C m⁻²) and Luvisol (13.2 ± 0.8 g C m⁻²) were much closer than the splashed sediments, indicating that erosion by splash preferentially moves lighter particles (i.e., high SOC content) (Beguería et al., 2015). In a field rainfall experiment in Spain, Beguería et al. (2015) found an empirical coefficient of 13 mg SOC relocated per gram of splashed sediment, with the highest SOC mobilization by splash for a sandy loam Gypsisol and the lowest for a silty Cambisol. The coefficients for our study are of the same order of magnitude: 44.3 mg TOC g⁻¹ splashed sediment for the Cambisol and 34.6 mg TOC g⁻¹ splashed sediment for the Luvisol. The higher coefficient for the Cambisol may be caused by the significantly higher SOC stock in the first 10 cm of soil (36.0 ± 4.0 Mg ha⁻¹ for the Cambisol vs. 23.4 ± 0.2 Mg ha⁻¹ for the Luvisol; Table 1).

Soil type also influenced PyC translocation by splash (Figs. 4b and 7). The smaller difference between the two soil types indicates that PyC erosion by splash depends much less on soil type than it did for runoff. Splash preferentially moves lighter particles (Beguería et al., 2015). Along the argumentation above for TOC, this effect can be related to the fact that PyC was available on the soil surface of both soils and the physical properties of PyC, such as the low density.

Finally, soil type was the main explanatory variable for vertical movement of PyC through the 10 cm soil column (Fig. 6). We found more PyC at 3–10 cm depth in the Cambisol than the Luvisol at the upslope position where PyC was initially added, as well as in the subsurface along the slope gradient. The higher vertical and subsurface mobility of PyC in the Cambisol compared to the Luvisol under unsaturated conditions (and excluding leaching of soluble parts) can be explained by higher infiltration rates for the Cambisol with high aggregate stability (Table 1 and Fig. S3). Therefore, more PyC was physically translocated (i.e., as particulate PyC or clay-sized PyC) with the percolating water running through larger soil pores (Hilscher and Knicker, 2011; Rumpel et al., 2015; Soucémarianadin et al., 2019). This vertical transport was limited in the Luvisol due to quicker surface sealing. The vertical movement of PyC depends largely on PyC size and solubility, but also on soil properties such as texture, aggregation, porosity and the infiltration rate (Abney et al., 2017), which in our study were more favorable in the Cambisol.

### 4.3.2 PyC characteristics

PyC characteristics (feedstock and particle size) was the second most important explanatory variable affecting PyC relocation.
<figure><img src="image_11.png" /><figcaption>**Figure 7.** Redistribution of PyC (%) through runoff and splash erosion and within the soil plots for all combinations of studied drivers (soil texture (Cambisol vs. Luvisol), slope angle (25° vs. 10°), PyC feedstock (grass vs. wood) and particle size (63 µm vs. 63 µm–2 mm)). Values represent averages per treatment (n = 3).</figcaption></figure>

distribution (Fig. 7). For PyC feedstock, however, we found contradictory results, in particular for wood PyC. On the one hand, there was more wood PyC transport by runoff and splash (sediment + floating particles) than grass PyC transport for both soils (% of total added PyC: 43.4 ± 6.6% for wood PyC and 28.4 ± 4.6% for grass PyC; Fig. 4). On the other hand, we also found more wood PyC than grass PyC on the soil surface (0–1 cm) in the upslope position where PyC was applied for both soils (fraction of OC derived from the PyC in percent (or PyC fraction): 11.5 ± 1.5% for wood PyC and 7.4 ± 1.0% for grass PyC; Fig. 6a–b), indicating that wood PyC either remained where initially applied or moved outside the 0.25 m² plot while grass PyC was redistributed more within the plot. The latter observation is in line with the general concept that grass-derived PyC has greater mobility than wood-derived PyC, which remains closer to its site of formation and initial deposition (Saiz et al., 2018). The higher mobility of grass PyC could be explained by its higher fragmentation potential due to the lack of strong physical structures of grass feedstock compared to wood feedstock (Pignatello et al., 2015; Singh et al., 2012). Wood feedstock is generally richer in lignin, and the resulting wood PyC is more crystalline and aromatic (Keiluweit et al., 2010; Singh et al., 2012), which was also the case for our PyC (Fig. S1). These differences can explain the higher retention of wood PyC compared to grass PyC on the soil surface at the upslope position of the plots, but not the greater relocation of wood PyC than grass PyC by runoff and splash. We assume

that this is caused by the greater fragmentation of grass PyC into smaller particles by raindrop impact. These smaller particles are more easily distributed in the soil, which makes them more difficult to detect based on δ¹³C and the proportion of PyC (few grams) to soil (several kilograms) (McCorkle et al., 2016; Pignatello et al., 2015). Overall, we found much more of the applied wood PyC than the grass PyC, for both PyC recoveries (% of total added PyC: 43.4 ± 6.6% for wood PyC and 28.4 ± 4.6% for grass PyC; Fig. 4) and PyC fraction (fraction of OC derived from the PyC in percent: 26.9 ± 4.9% for wood PyC and 17.7 ± 3.8% for grass PyC; Fig. 6), which supports this assumption. Spokas et al. (2014) further observed the same or higher levels of fragmentation for wood-derived feedstocks (lignin-rich) compared to grass-derived feedstocks (cellulose-rich), depending on the experimental conditions applied. Our different findings ultimately indicate that both the fragmentation potential and the mobility of PyC do not only depend on the feedstock material (grass versus wood) but also other factors such as surface area, porosity, induced mechanical stresses, etc. (Crawford and Belcher, 2014; Singh et al., 2012; Spokas et al., 2014).

For the runoff and splashed sediment (without floating particles), the mobility of fine PyC particles was larger than for the coarse particles (Fig. 4a–b). This finding is in line with the greater retention of coarse PyC particles on the soil surface (0–1 cm) in the upper part of the plot where PyC was added, especially for the Cambisol (Fig. 6a–b). Particle size can be a key driver of long-distance transport of PyC. It is
generally assumed that the surface transport potential and ef-
ficiency is greater for finer PyC particles and they are there-
fore transported over longer distances (off-site export) than
coarser particles that remain closer to the site of formation
(Abiven and Santín, 2019; Masiello, 2004; Saiz et al., 2018;
Tinner et al., 2006). Finer PyC particles also remain in sus-
pension for a longer period of time as they settle from the
mixture more slowly (according to Fick's law) (Rumpel et
al., 2015). Since the particle size determines PyC suscepti-
bility to erosive transport, fragmentation after initial depo-
sition (and during transport) can increase the transport po-
tential of PyC particles. Higher fragmentation of grass PyC
into smaller particles could ultimately lead to higher mobil-
ity (Pignatello et al., 2015; Rumpel et al., 2015). Only for
the separated floating particles eroded by runoff and splash
(Fig. 4c–d) were the coarse PyC particles more prevalent.
The larger quantities of coarse PyC in the floating particles
of runoff and splash are caused by the higher floating poten-
tial of coarser PyC, likely due to its low density and high
porosity (Rumpel et al., 2015).

4.3.3 Slope

Slope angle had a minor effect on the mobilized quantities of
soil, SOC and PyC and was only significant for the Luvisol,
where a slope of 25° resulted in increased soil and TOC, but
not PyC erosion by runoff (Figs. 2–4). As slope was only
relevant for the Luvisol and only for particles transported
by runoff, it could be related to the greater runoff ratio and
therefore surface transport for the Luvisol under a 25° slope.
Several studies have confirmed the limited effect of slope on
PyC redistribution (Boot et al., 2015; Cotrufo et al., 2016;
Galanter et al., 2018), but it is important to note that slope
angle may be more important on larger plots or along hill-
slopes where slope angle can be assessed together with slope
length and aspect (Abney and Berhe, 2018; Shakesby et al.,
2015). These two topographic features could not be assessed
in our plot-scale study.

## 4.4 Consequences for understanding PyC redistribution in the landscape after fire

Our findings regarding the factors that affect PyC relocation
during simulated rainfall events advance our understanding
of PyC redistribution in the landscape. We show that PyC
was highly mobile and quickly transported and relocated on
0.25 m² plots during 30 min of intense rainfall. Our exper-
imental study was done under controlled conditions, which
partially limits a direct comparison of our data to natural
hillslopes. To fully understand PyC redistribution and depo-
sition in the landscape after a fire, it is therefore of great
importance to assess initial post-fire rainfall events and to
track PyC relocation by erosion at the hillslope and catch-
ment scales (Cotrufo et al., 2016; Masiello and Berhe, 2020).
In particular, the plots used in this study are much shorter

than real hillslopes and therefore do not account for long-
distance transport (Rumpel et al., 2006). For longer hill-
slopes, slope steepness, length and aspect, and post-fire sur-
face roughness but also micro-topographic features such as
depressions or the formation of rills and gullies affect the
effective infiltration rates and transport capacity of overland
flow, and thus runoff erosion and PyC redistribution. With
increasing hillslope steepness and decreasing surface rough-
ness (due to removal of ground cover after a fire), surface
runoff and PyC transport will likely increase; with increasing
hillslope length, the transport capacity of overland flow gen-
erally declines, which increases the chances that PyC is de-
posited along the slope or in lower-lying areas of catchments
and can ultimately enter the soil (Abney and Berhe, 2018;
Masiello and Berhe, 2020). In this regard, it has to be noted
that not only runoff erosion will likely change on longer hill-
slopes, but also the interaction of runoff and splash erosion.
With our methodological approach, we could not fully sep-
arate these two processes, and parts of eroded material by
splash accounted for runoff erosion since they occurred on
the soil plots themselves in the direction of the slope, which
favors its final export by runoff.

In addition, the results will be different for real post-fire
landscapes because of the heterogeneity in ground cover
and soil hydrological and physical properties of fire-affected
(burned) soils. Fire-affected soils are affected by changes in
i.e., vegetation cover, hydrophobicity, water repellence, in-
filtration or aggregate breakdown (Abney and Berhe, 2018;
Moody et al., 2013; Shakesby, 2011). The fire regime (sever-
ity, intensity and frequency) will determine the fuel con-
sumption, as well as PyC production and characteristics
(Bowman et al., 2009; Santín et al., 2015). In our experiment,
we used unburnt soil without ground cover except for the
added PyC. Fires remove substantial proportions of ground
cover (up to 90%), but after an actual fire the soil surface
may be covered with debris, ash, charcoal or partially burned
plant material, which will lead to a patchy ground cover (Jo-
hansen et al., 2001; Pierson et al., 2013; Shakesby and Do-
err, 2006). In our study, both the soils (very hydrophilic) and
PyC materials (extremely hydrophobic) were similarly wa-
ter repellent (Tables 1–2). On real fire-affected hillslopes,
burnt soils will likely be more water repellent, leading to
more runoff and likely more transport of particles and PyC
(DeBano, 2000). Fires can also change the water-holding
capacity of soils and soil chemistry (Fonseca et al., 2017;
Moragues-Saitua et al., 2017; Robichaud et al., 2016). How-
ever, we did not change the soils’ physical structure (i.e., ag-
gregation or porosity) prior to rainfall experiments, except
that we slightly smoothened the surface. Burned soils may
strongly be affected by changes in aggregation, porosity and
therefore infiltration capacity due to heat-induced aggregate
breakdown, volatilization or charring of organic matter, or in-
wash of particles, such as ash or PyC, resulting in more pore
clogging and surface sealing than in our experiment (Certini,
2005; Jian et al., 2018). However, limited clogging through
washin of ash or PyC has also been found (Stoof et al., 2016). Even though we did not account for these changes in fire-affected soils, our results of PyC redistribution are relatively comparable with plot-scale studies using burnt soils in the field (Rumpel et al., 2009).

Precipitation also has a great influence on post-fire erosion dynamics but is highly variable in nature and depends on local to regional climatic conditions. Although rainfall simulation experiments on plots are essential to understand individual processes during single erosion events due to high level of control and comparability, they are limited in spatial and temporal extent (Clarke and Walsh, 2007; Doetterl et al., 2016; Iserloh et al., 2012). PyC redistribution after rainfall will not be uniform in time and space, and it is therefore important to use multiple successive events in future studies to take this temporal and spatial evolution into account (Moody et al., 2013). Using longer rainfall durations or successive rainfall events would likely have resulted in parts of the remaining PyC on the soil surface to be further relocated by runoff and splash, but probably to a much lesser extent. Longer rainfall events could facilitate redistribution of PyC that had already entered the soil column after 30 min. A lower rainfall intensity would likely have led to less overland flow and reduced transport by runoff, but possibly still substantial PyC redistribution due to preferential relocation of low-density particles like PyC. An even higher rainfall intensity would likely have led to more overland flow and increased sediment and PyC transport (Moody et al., 2013; Rumpel et al., 2015). Higher rainfall intensities or longer durations could likely further facilitate breakdown of PyC particles due to the impact of the raindrops, subsequently increasing its mobility.

Despite the limitations of these experimental settings, controlled conditions and multi-factorial experiments are crucial for our understanding of key drivers of PyC redistribution. The data and findings of this study give directions for larger-scale field studies and help generalization of model parameters. In particular, our results clearly show that soil type affects the mobility of PyC (Fig. 7). PyC export is less for a fine-textured well-aggregated soil than for silty soil with poorer aggregate stability. This result is in line with the notion that soil properties, together with key hydrological drivers, determine the spatial variability of PyC in soils at the landscape scale (Rumpel et al., 2009; Soucémarianadin et al., 2019). Our findings indicate that PyC redistribution depends on the feedstock from which it was derived (Fig. 7). Both wood and grass PyC can be highly mobile, depending, at least partially, on its particle size. PyC relocation may be greater for grassland-dominated than tree-dominated catchments because grass PyC is smaller and more susceptible to fragmentation, therefore potentially breaking apart into even smaller pieces that are more mobile (Pignatello et al., 2015; Saiz et al., 2018). Consequently, vegetation cover determines the feedstock for PyC production, which in turn will likely govern the size, stability and therefore mobility of PyC (Saiz et al., 2018). This needs to be taken into account for field in-

vestigations and for modeling of PyC erosion at the hillslope or catchment scale. In addition, our results suggest that the presence and redistribution of PyC in the landscape can affect soil organic matter mobilization. We showed that nSOC export changes in the presence of PyC, but the processes that cause these changes could not be assessed and need further study.

## 5 Conclusions

The rainfall simulation experiment on 0.25 m² soil plots presented here shows that large quantities of PyC can be redistributed during a short period of time. Between 3.7 ± 1.0% and 73.4 ± 3.8% of the initially added PyC was redistributed by runoff and splash during a 30 min high intensity rainfall event. Soil texture, slope angle, PyC feedstock and particle size affect the mobilization of PyC to a different extent. Soil type substantially influences the redistribution of PyC at the plot scale, probably due to differences in texture, aggregate stability, and SOC contents. For the studied Cambisol, only a little PyC was moved with runoff or splash, and significantly more PyC remained on the plot where it was initially applied or moved vertically into the soil. For the Luvisol, large quantities of PyC were moved with runoff and splash, but only a little PyC moved vertically into the soil column. Furthermore, the erosional behavior of wood and grass PyC differed, suggesting that this must be taken into account when determining post-fire erosion budgets for catchments under different vegetation. While more wood PyC was mobilized by runoff and splash than grass PyC, also more wood PyC was retained on the surface where it was initially applied. Alongside PyC feedstock, particle size also influences the mobility and off-site transport of PyC. Relocation of PyC may be greater for grass-dominated ecosystems because grass PyC is initially smaller and also more susceptible to fragmentation; the finer PyC, the more susceptible to redistribution. Slope angle had only a minor effect on PyC relocation at the plot scale but must be taken into account for larger scales, such as hillslopes or catchments. Finally, the presence and relocation of PyC affected the mobilization and export of native SOC.

The identification of the relative importance of these individual drivers of PyC redistribution will help to improve the design of more time- and cost-intensive field studies. Our simulation experiments can also provide crucial inputs to simulate the fate of PyC in landscape or Earth system models. However, further research is needed to understand the importance of key drivers of PyC redistribution at larger scales, such as hillslopes or catchments, in order to explain the spatial heterogeneity of SOC and PyC stocks in the landscape.

*Data availability.* The data related to this article are available at https://doi.org/10.5281/zenodo.4422514 (Bellè and Abiven, 2021).
*Supplement.* The supplement related to this article is available on-line at: https://doi.org/10.5194/bg-18-1105-2021-supplement.

*Author contributions.* SA acquired the funding. SB and SA conceptualized the study. SB conducted the experiment, analyzed and visualized the data, and wrote the manuscript, and all authors commented on the manuscript.

*Competing interests.* The authors declare that they have no conflict of interest.

*Acknowledgements.* The authors acknowledge the support and ability to use the facilities at the Swiss Federal Institute for Forest, Snow and Landscape Research (WSL), especially Manfred Staehli and Werner Gerber. We further thank Thomas Keller (University of Zurich) for technical assistance.

*Financial support.* This research has been supported by the Swiss National Science Foundation (grant no. 200021_178768).

*Review statement.* This paper was edited by Yakov Kuzyakov and reviewed by Diana Vieira and one anonymous referee.

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