Understanding the drivers of the boreal forest fire activity is challenging due to the complexity of the interactions driving fire regimes. We analyzed drivers of forest fire activity in Northern Scandinavia (above 60 N) by combining modern and proxy data over the Holocene. The results suggest that the cold climate in northern Scandinavia was generally characterized by dry conditions favourable to periods of regionally increased fire activity. We propose that the cold conditions over the northern North Atlantic, associated with low SSTs, expansion of sea ice cover and the southward shift in the position of the subpolar gyre, redirect southward the precipitation over Scandinavia, associated with the westerlies. This dynamics strengthens high pressure systems over Scandinavia and results in increased regional fire activity. Our study reveals a previously undocumented teleconnection between large scale climate and ocean dynamics over the North Atlantic and regional boreal forest fire activity in Northern Scandinavia. Consistency of the pattern observed annually through millennium scales suggests that a strong link between Atlantic SST and fire activity on multiple temporal scales over the entire Holocene is relevant for understanding future fire activity across the European boreal zone.
Fire is a primary driving factor of the ecosystem dynamics in the boreal forest, directly affecting global carbon balance and atmospheric concentrations of trace gases including carbon dioxide1,2. Large areas of the boreal forest that burn annually in North America (predominantly in Canada) and Eurasia (predominantly in Russia) exemplify a fundamental link between large scale atmospheric circulation processes and fire regimes3,4. Fires in the boreal region are estimated to represent around 9.1% of the annual total biomass burned globally5. Studies in the Eurasian boreal forest show that fire releases 4.8 to 15.4 Tg C/ha depending upon size and severity6. Climatically and human-induced changes in fire regimes impact the functioning of the boreal ecosystem by affecting regeneration and growth conditions for dominant tree species, forest composition and its successional pathways7.
Under natural conditions, climate is the major factor controlling fire activity as large-scale circulation patterns determine periods of fire-conducive weather and synchronize fire regimes across landscapes and regions of the boreal zone8,9. Human activities have also impacted forest fire regimes10 through the use of fire for agricultural purposes such as slash-and-burn agriculture and, more recently, through fire suppression. Modern human impact results in a decrease in natural fire activity, even though increasing human densities are linked to a higher density of ignitions. Although in Scandinavia forest fires been historically one of the principal factors shaping the forests’ state and function11,12, forest fire activity in Northern Europe has been decreasing since the late 19th century13.
The European climate is largely determined by heat and humidity transfer from the adjacent North Atlantic Ocean, notably through the warm and saline North Atlantic Current (NAC) flowing northeastward14,15,16. The influence of the strong NAC results in relatively high winter temperatures and lower seasonal temperature contrasts as compared to the regions at similar latitudes in North America. Large scale circulation anomalies affecting the energy balance of the northern North Atlantic Ocean and associated atmospheric pressure patterns have been repeatedly shown to affect European weather17,18,19. Historically, however, most of the analyses have been focused on the winter climate, since it is the period when ocean-weather feedback appeared to be the most pronounced20. It is reasonable to hypothesize that the process affecting the humidity and energy transport over the North Atlantic Ocean should be equally important for the summer climate and, therefore, regional fire activity. Indeed, the summer temperatures and precipitation dynamics over Scandinavia have been shown to be largely controlled by the position of the westerly tracks and the strength of NAC21. Studies in different parts of the world have shown strong linkages between regional fire activities and changes in sea surface temperatures (SST) and the associated pressure patterns controlling precipitation over adjacent lands22,23,24,25,26,27.
In this paper, we hypothesized that ocean conditions in the northern North Atlantic play a determinant role on regional fire activity in northern Scandinavia28. We propose that a weakening of the NAC and stronger regional winter cooling, reflected by colder SST in the North Atlantic, would result in increased fire activity in the following fire season. We tested this hypothesis using modern forestry data on annually burned areas in northern Scandinavia (north of 60°N), multi-century and spatially-explicit dendrochronological reconstructions of annually burned areas, reconstructions of surface air temperature (SAT) and fire activity and reconstructions of sea surface conditions (SST and sea ice cover) over the northeastern North Atlantic during the Holocene.
The study region
The main study region covered the area of northern Sweden between 60°N and 70°N. It lies in the boreal climatic zone and receives air masses from the Atlantic region, especially during the winter season, which makes it particularly sensitive to the strength and thermal properties of NAC. Hence, despite the high latitudes, the mean January temperature ranges between −4 to −16 °C and the mean July temperature ranges from 12 to 16 °C. The number of days with a mean temperature above 5 °C ranges between 100 and 16029. The total annual precipitation is 600–700 mm on average, but with very high variability at higher elevations where it ranges between 400 and 1400 mm. Snow accounts for 30% to 50% of the annual precipitation and covers the ground for an average of 170–225 days/year29. The majority of modern forest fires in northern Sweden occur early in the fire season (May through June), although the total burned area is dominated by August fires13. Northern Sweden encloses the alpine zone, north, mid- and south boreal forests30. Scots pine (Pinus sylvestris L.), Norway spruce (Picea abies (L.) H. Karst) and birch (Betula pubescens Ehrh. and B. pendula Roth) are the dominant species in the forest vegetation cover. Fire has been the primary disturbance factor in this boreal ecosystem with stand-level fire return interval in mixed pine forests ranging between 30 to 100 years12. The modern (second half of the 20th century) fire cycle in the northern part of Sweden is 103–104 years13, which is attributed to efficient fire suppression policies.
Rationale and dataset selection
The starting point in the analyses was a pattern shown in a previous study, which demonstrated a relationship between major fire years in northern Scandinavia and regional positive temperature and negative precipitation anomalies28. We hypothesized that the fire pattern arises from large scale anomalies in atmospheric circulation, extending far outside the study region and beyond the fire season. The fact that the observed precipitation and temperature anomalies extended over most of the summer suggested that they were likely related to changes in energy states of the atmosphere and ocean surface. Accordingly, we extended the geographical frame of our analyses over the North Atlantic and included the winter and spring months preceding the start of the fire season. We tested the link between the surface ocean temperatures and fire activity at annual, centennial and millennial scales. Detailed analyses of spatial relationships were made using modern data from the 20th century. We also extended the time interval for the analysis to the last 8000 years to analyse long-term changes but still avoiding climate perturbations related to the glacial-interglacial transition. Eight thousand years ago also roughly coincided with the start of paleo fire records in the study area (Supplementary Information Table SI 1).
In our long-term analyses, we largely capitalized on tree-ring and chironomid-based summer temperature reconstructions even though we realized that aridity records (e.g. precipitation) may provide equally important information about changes in historical burn rates. Reliable and sufficiently long paleo-aridity records are, however, not yet available for our study region. Seasonally-resolved precipitation records from tree rings are only available for the past few centuries31,32 and do not contain centennial signal33. Some precipitation records from lake sediment data are resolved with decadal resolution, but cover only a part of the Holocene34,35. By contrast, air temperature records from northern Sweden are available with seasonal (e.g.36) to decadal-centennial resolution for the entire Holocene37.
Fire records with annual resolution
For the analyses of fire at annual scale, we used modern forestry statistics and dendrochronological fire reconstructions. Forestry statistics provided data on the annually burned forested areas in northern Sweden from 1942 to 1975 and from 1996 to 201413. The composite fire record did not exhibit temporal autocorrelation (|r| < 0.10 for time lags up to 15 years).
Dendrochronological fire reconstructions, which aimed at extending annually-resolved fire records over centuries, were based on assigning the exact calendar year (crossdating) to fire scars in the wood of Scots pines (Pinus sylvestris L.). We used two dendrochronological datasets. First, we developed spatially explicit reconstructions of fire activity (amount of area burned annually) at two sites in northern Sweden, one since 1320 AD (site Bjurholm, area 60 800 ha, Fig. 1, Table SI 1) and the other from 1371 AD (site Tiveden, area 1200 ha). For both areas, we used the network of sites with independently reconstructed fire histories from tree fire scars. We considered properties of major fire breaks (e.g. lakes and rivers) and distribution of burned and unburned (and recording) sites across the landscapes to determine the size of each fire (for the detailed methodology, see38). Second, we used a previously published list of years which were shown to exhibit high fire activity at the regional scale (so-called large fire years, LFYs), identified by contingency analyses on a northern Swedish network of fire history sites (Fig. 1; Table SI 1 39). LFYs account for the majority of the forest burned area at decadal-centennial time scales40. LFY were identified using both the percentage of sites burned in a year and the theoretical probabilities of observing a particular number of areas burned in a year. We then assessed the theoretical probabilities though contingency analysis, considering fire activity as a realization of a binominal process:
where N was the total number of recording areas in the analysis of a specific period; X – the number of burned areas in a single year; p – the probability of an area burning in any year and q – the inverse of this probability. The differences between expected and observed frequencies were estimated with the Chi-square test (Sokal and Rolf 1995). We refer to28 for the details of this analysis.
Fire records at above-annual resolution
As a proxy of forest fire activity in the past, we used charcoal concentration data from three 14C dated lake sediment cores from Northern Sweden (Fig. 1, Table SI 1 41). The cores were calibrated on age-depth models and were transformed to the same and constant time resolution (20 years41). We averaged the data from these sites through a standard two-step smoothing procedure using R package paleofire42 and converted the data into charcoal influx binned into 200 year intervals. Prior to averaging, the site chronologies were standardized to ensure that equal weights were attributed to each site in the master chronology.
Surface air temperature (SAT) paleo reconstructions
As a source of annually resolved summer (May-August) temperature records over the last millennium, we used a reconstruction from the Torneträsk area in northern Sweden (Fig. 1), which included tree ring-width and maximum density measurements36. To extend back the temperature records over much of the Holocene, we used reconstructions of summer (May-September) temperatures based on the analysis of chironomid and diatom assemblages recovered from sediment cores of two lakes in Abisko Valley (Lake830 and Lake Vuoskku), northern Sweden37. Similar to the treatment of charcoal data, the initial chronologies were standardized and converted to the same temporal resolution (200 years) prior to averaging, to obtain a composite temperature record.
Modern records and proxies of atmospheric and ocean variability
We used satellite-based sea-ice concentration data from the National Snow and Ice Data Center, Boulder Colorado US43, for the interval overlapping of the modern fire data (1996–2014). Sea-surface temperatures (SST) since 1870 were obtained from the UK Met Office Hadley Centre observations datasets44. We obtained monthly geopotential 500 hPa pressure heights (~200 km2 grid scale) from the NCEP/NCAR Reanalysis product from 1948 to 201445,46. To represent fire-conducive weather conditions over the periods longer than those covered by fire statistics, we used a monthly 0.5° gridded dataset of self-calibrated PDSI (version 3.2147) over a northern Sweden area (60–64 °N and 4–14 °E), which are available for 1880–2010. In addition, we used monthly 0.5° gridded precipitation and temperature data (1901–2013) from the CRU TS3.22 dataset48.
As a paleo NAC strength indicator, we used an alkenone-based SST reconstruction from the Vøring Plateau, Norwegian Sea (core MD95201149). We also used two reconstructions of North Atlantic drift ice, available from coring sites in the northwestern (core KN158-4GGC22) and northeastern (core VM29-191) North Atlantic50. Percentages of Icelandic glass and percentages of hematite-strained grains were used as proxies for ice rafted debris (IRD) available from these sites. These chronologies were converted to the same temporal resolution (200 years), standardized and averaged to obtain a site-specific record of drift ice since 8000 cal years BP. We also used a dinocyst-based reconstruction of seasonal sea ice cover extent in the Labrador Sea (core HU84-030-021)51,52.
We correlated (by using Pearson correlation) the chronology of 20th century annually burned areas in Northern Sweden with each point in the SST and 500 hPa pressure fields for the area limited by 20–80° N and 80°W–30°E and for the periods 1948–1975 and 1996–2014. Prior to the analyses, the fire data were log- and square-root transformed to ensure the normality of the distribution. Statistical significance of the correlations was tested through a two-sided Student t-test, with autocorrelation in the time series being taken into account through adjusting the critical values for the t-test53. For each correlation map, we also calculated field significance, a measure of correlation strength at the scale of the studied geographical area54.
Annual burned areas reconstructed from dendrochronological data were transformed to cumulative amounts over a moving average of 100-years with 10-year shifts, calculated over the period from 1350 (1400) to 1900 AD. This step resulted in smoothed fire chronologies at 10 year resolution to be used in regime shift analysis. The temporal limits of the analyses were defined by data availability (the start of the period) and the onset of fire suppression (the end of the period). The list of LFYs over the an area Northern Sweden, defined an LFY on the basis of contingency analyses and the synchronicity threshold over 1270–1914 AD39 was used in conjunction with the normalized tree ring-based reconstruction of summer temperature36. To this end, we computed the mean number of LFYs during “cold” and “warm” periods, as identified by regime shift analyses (see below) and then randomly shuffled the result with the replacement of the LFY occurrences 1000 times, thus obtaining a bootstrapped null distribution of random LFY occurrence during each of the warm/cold periods. We then constructed a 95% confidence interval around means and evaluated the statistical significance of the deviation of the observed empirical value as compared to the number expected under the assumption of random LFY occurrence.
To evaluate the spatial pattern of deviations in the Atlantic SST and pressure fields during 20th century LFYs, we used superposed epoch analysis (SEA55). We selected the five LFYs known from the modern forestry statistics (years 1901, 1933, 1959, 1969, 2014)13. Although the replication for the SEA analyses was low, one should acknowledge an inevitable compromise between the notion of large fire year (i.e. how intense the fire activity should be to qualify a year as a large fire year, LFY) and the number of such years in analysis. Taking a more conservative approach towards the definition of LFY we therefore adopted a more opportunistic approach towards number of years, considered acceptable for the analysis. SEA analyses were done with the KNMI Climate Explorer tool53,56. SEA is based on aggregating data from years with a particular outcome (e.g. years with large forest area burned, LFY), averaging that data and assessing significance of the departure of that average value from the mean calculated on the complete sampled distribution of the variable in question57. The method is designed to test for consistency in the response of a variable under or during a discrete event or factor, with significance being tested through bootstrapping or evaluating distribution of the complete sampled distribution.
To investigate the agreement of temporal changes in fire activity and those in reconstructed air and ocean temperature changes, we used a regime detection algorithm58. The algorithm focuses on the detection of time points of changes in the mean values of the respective time series and uses the Regime Shift Index (RSI)59, which is calculated for each point (c) of time series:
where m = 0, …, l – 1, with l as a cut-off length of evaluated regimes; σl is the average standard deviation for the complete set of one-year intervals in the original time series; and xi* is a normalized deviation from the hypothetical mean level for a new regime.
To test for statistical significance in the RSI changes, the method relies on sequential t-tests, subsampling (Monte Carlo technique) and bias correction, which includes least squares estimates of the serial correlation to provide robust estimates of the significance of changes in the means60. A significance level of 0.1 and Huber’s weight parameter of 1, which controlled for weights assigned to outliers, were adopted for all of the analyses. This setting can be viewed as a threshold below which the sensitivity of the algorithm to detect potential changes progressively declines. Red-noise estimation was done through ordinary least squares estimation with data prewhitening with the length of sub-sample size being equal to 50% length of the defined cut-off.
We applied the algorithm independently for each of the analyzed time series: the northern Swedish fire activity, summer SAT reconstructions, eastern North Atlantic SSTs, IRD and Labrador sea ice cover chronologies. The analysis was performed for two time scales. For the dendrochronological reconstructions of annually burned areas (sites Bjurholm and Tiveden) and northern Scandinavian summer SAT, we used a 100 year cut-off length. For the SSTs, lake temperature estimates and charcoal-based fire reconstructions over the Holocene, the cut-off was set at 800 years. Prior to the analyses, SAT, SST and IRD reconstructions were detrended by subtracting the long-term linear trend in order to suppress the influence from any trend over the entire analysis period.
Relationship between modern fire activity, SST and 500 hPa pressure heights
Over the 20th century, the annually burned area in northern Sweden correlated negatively with SST variations in parts of the extratropical Atlantic Ocean (Fig. 2). The region with the highest correlation (r in the range of −0.3 to −0.6) was observed within 50–40°W and 40–50°N, which is close to the Grand Banks, an area marked by a front between the Labrador Current and the NAC. The correlation was highest for April-May, which is the period of the year following the maximum sea ice spread in the northwest North Atlantic and immediately preceding the fire season. It persisted over the June through August, somewhat diminishing zonally by extending along the eastern coast of North America. The SST variability in April-May within the region off the Grand Banks accounted for nearly 40% of the variability in burned areas (Fig. SI 1A). Moreover, a moving correlation analysis indicated that the pattern was temporally stable (Fig. SI 1B). Although analyses of teleconnection between Northern Atlantic SSTs and fire activity showed moderate levels of significance at the scale of the selected geographical area (pfield < 0.05–0.20), this is a result of a limited geographical extent of the likely “centre of action” near the Grand Banks (an area surrounded by 40–50° N and 50–40° W) and the vast area included in these analyses (20–80° N and 80W–30°E). Consistently low p values in that “center of action” (p < 0.005, Fig. SI 1C) support the notion of teleconnection between North Scandinavian fire activity and SSTs.
Superposed epoch analysis based on the five LFY in the modern fire record (1959, 1966, 1969, 1997 and 2014) applied to the SST field pointed to the same important region of northern North Atlantic. However, the geographical and temporal extent of significant SST anomalies was more geographically limited than for the correlation analysis on the entire record and it was temporally restricted to April-June (Fig. SI 2).
There was a strong negative relationship between sea ice cover extent and SSTs in the northwest North Atlantic (r ~ 0.4–0.6, Fig. 3A), especially during the winter and spring. Therefore, we calculated the correlation between February-April sea ice concentrations in the Grand Banks areas and the burned areas: in the 48–52°N and 53–48°W region, a strong positive correlation linked the two variables (r ~ 0.5–0.7, Fig. 3A).
The negative relationship between SST and annually burned areas suggested that there might be a general relationship between SSTs in parts of the North Atlantic and the summer aridity of Northern Scandinavia. To test this hypothesis from modern instrumental data, we correlated the self-calibrated Palmer Drought Severity Index (PDSI) in July-August over Northern Sweden in the 60–64° N and 4–14° E region with Atlantic SST for April-May (Fig. 3B). The results suggested that a warmer extratropical North Atlantic was associated with higher PDSI, which corresponds to more humid and less fire-prone conditions in northern Sweden. Because the choice of the geographic region to analyze affects the results, we also ran the analysis using SSTs averaged over the area limited by 40 to 50°N and 50 to 40°W and correlated them with PDSI at each grid point over the whole Scandinavian Peninsula (Fig. 3C). The observed pattern showed a positive relationship between April-May SST and summer humidity for parts of the region, with the strongest teleconnections observed in southeastern Sweden, northern Sweden and northern Finland. The precipitation dominated this relationship (Fig. SI 3). During the 1900s, the annually burned areas in northern Sweden were correlated with precipitation rather than with temperature (Fig. SI 3A vs SI 3C).
During the fire season, high pressure systems dominated over Scandinavia and the British Isles, according to the SEA analysis (Fig. 4, Fig. SI 4). During the winter months, years with an anomalously large area burned were associated with negative anomalies in 500 hPa pressure heights, centred around 55° N across the Atlantic. Low pressure systems later developed over the Davis Strait, southern Greenland and northern Quebec during the spring (Fig. 4). Correlation analyses between 500 hPa pressure heights and annually burned areas, operating on the modern record, including both LFY and non-LFYs, revealed generally similar but a statistically less pronounced pattern (Fig. SI 4).
Relationship between fire activity and temperature variability over 1400–1990 AD
Annually burned areas reconstructed at the Bjurholm and Tiveden sites revealed temporal synchronicity according to the regime shift analysis (Fig. 5), despite differences in the levels of average fire activity and site areas (Table SI 1). Fire prone intervals included the 1600s at both sites and the 1800s for the Bjurholm site only. Lower average levels of fire activity were observed during the 1400–1600 period (1500–1600 in the shorter Tiveden record) and during the 1700s. Increased fire activity occurred during colder periods, as suggested by the regime shift detection algorithm applied independently to the tree-ring based temperature reconstruction (Fig. 5)36. Between1300 and 1880, LFYs occurred significantly more frequently during the cooler than warmer periods, according to the bootstrap analysis. The empirical difference between the number of LFYs in cold and warm periods (7) was larger than the 99.9% quantile (5) of the bootstrapped (n = 1000) distribution of that difference under the assumption of random LFY occurrence.
Fire activity and environmental variability at Holocene scale
Northern Swedish fire activity since 8000 cal years BP as reconstructed from sediment charcoal41 tended to be inversely associated with chironomid-based July temperature estimates37 (Fig. 6), according to the regime shift analysis. Increased charcoal fluxes occurred between 8000 and 7000 cal years BP, 6000–5500 cal years BP and since 3000 cal years BP. The two later intervals were associated with colder conditions, except for the earliest period when higher fire activity coincided with a warmer climate. However, increased fire activity broadly coincided with lower SST in the Norwegian Sea as inferred from alkenone-based reconstruction of core MD95201149 in all three intervals.
Sea ice cover reconstruction of the Labrador Sea from core HU84-030-021 revealed three periods of increased ice cover since 8000 BP, according to regime shift detection analysis (Fig. 6). These were 8000–7000 BP, 6000–5000 BP and since 4000 BP until the present time. Increases in Labrador ice cover broadly coincided with increases in fire activity reconstructed from lake sediments in Northern Sweden. Although we observed a limited synchronicity between the Labrador ice chronology and the charcoal-based reconstruction of Scandinavian fire activity over 4000–3000 BP, we noted that during the latest period with increased fire activity (since 3000 calBP), the majority of data points representing ice reconstructions indicated above average ice concentrations.
Records of IRD, related to sea ice spreading in the northwestern (core KN158-4 GGC22) and eastern North Atlantic (core VM29-191), together with sea ice cover reconstruction from the Labrador sea (core HU84-030-021), indicated increases in winter sea ice concentration and its areal extent around 8000–7000 and 6000–5200 cal years BP. Both intervals coincided with increased fire activity in Northern Sweden (Fig. 6), although the regime shift analysis did not show the IRD index in the period since 3000 BP as significantly different from that between around 3000–5000 BP.
The correlation between the 20th century fire activity in northern Scandinavia and SST and sea ice cover in the northwest North Atlantic pointed to a teleconnection between ocean conditions and the fire conductive weather of Northern Scandinavia. The oceanic region with the highest correlation is located off the Grand Banks, which is a critical area in the North Atlantic circulation due to the cold Labrador Current, flowing southward and making a front with the warm North Atlantic Current (NAC) flowing northeastward61,62. Hence, increased sea ice spread and freshwater export via the Labrador Current into the NAC61 may induce reduction of the Atlantic Meridional Overturning Circulation (AMOC). Superimposed epoch analyses on the northern Swedish LFYs during the 20th century, suggested a close relationship of regional fire activity with winter sea ice cover and development of low pressure systems at the winter-spring transition (February-March) in the subpolar North Atlantic, further promoting southward sea ice transport from the Labrador Sea. A strong correlation between the annually burned area in Northern Sweden and the sea ice concentration off Newfoundland during the winter-spring months supported the hypothesis of a teleconnection between the oceanography of the northwest North Atlantic and hydroclimatological conditions in Scandinavia. Analyses of historical hydrographic data, reconstruction and modelling studies together suggest that sea ice and freshwater export through the Labrador Current is one of the important factors controlling the properties of the NAC at annual61, decadal63,64, centennial65,66 and millennial time scales50. The increased flow of cold and low saline Arctic water into the western North Atlantic weakens the NAC and leads to a southward shift of the western storm tracks67 fostering the development of high pressure systems over northern Europe (Fig. 4) with dominant dry Arctic air masses in summer. This is consistent with the negative correlation between summer aridity over most of the Scandinavian Peninsula and the average April-May SST in the northwest North Atlantic (Fig. 2A). This is also consistent with the results of modelling experiments simulating the response of the freshwater discharges on large-scale wind fields over the northern North Atlantic65. The critical role of North Atlantic SST and NAC on the aridity of Northern Europe has been further demonstrated from oxygen isotope data in late Holocene lacustrine record of Swedish Lapland: δ18Osi depletion events related to shifts in precipitation source from Atlantic δ18Osi - rich air masses to dryer Arctic air masses were concomitant with the IRD maxima in the northern North Atlantic68.
Changes in pressure fields over the North Atlantic apparently amplify the effect of SST on fire activity in northern Europe. Correlation analysis on SST fields suggested a strong relationship between average SST conditions and fire activity (Fig. 2) while showing a much weaker signal with respect to LFYs in SEA analyses (Fig. SI 2). The pattern was reversed in the analyses of 500 hPa pressure heights, which revealed a much stronger pattern during LFYs (SEA analysis, Fig. 4) than correlation analyses on the complete dataset (Fig. SI 4). We speculate that the relative contribution of SST dynamics vs. changing pressure patterns over the Northern Atlantic on fire activity in Northern Europe vary along a gradient in the regional fire hazard, with pressure anomalies being increasingly important during years of generally colder SST in the North Atlantic. Along with internal cycles and feedbacks within the subpolar gyre66,69, external forcings have been suggested to affect the flow of cold Arctic water to the northwest North Atlantic50,70,71. Based on detailed paleoceanographic reconstructions, linkages have been proposed between the decline in solar irradiance and the blocking of high pressure systems that modified storm tracks and weather over Western Europe72.
Annually burned areas dendrochronologically reconstructed for two areas in northern Sweden revealed strong synchronicity at centennial time scales. We observed increased fire activity during the 1600s and most of the 1800s, which were marked by surface air temperatures below average as independently reconstructed from tree-ring data (Fig. 5)36. This includes the coldest interval of the Little Ice Age (LIA) that was recorded in Scandinavia during 1600s. Cold intervals exhibited a higher frequency of LFYs as identified through synchronicity analysis of the North Sweden-wide network of fire history sites. We, therefore, propose that cool climate periods in Scandinavia were associated with low atmospheric humidity and increased frequency of high pressure systems dominated by cold and dry air masses. Such a hypothesis is supported by sunshine reconstruction in Fennoscandia indicating generally sunny summers during the LIA but cloudy conditions during the Medieval Warm Anomaly73. The negative correlation between surface air temperature and fire activity reported for the Northern Europe may not be unique. An increased fire frequency during the LIA has been reported from dendrochronological reconstruction in the boreal forest of Western Quebec and related to an increase in summer aridity74.
Colder periods in northern Scandinavia might be more prone to climatic extremes as compared to warmer periods, probably as a result of more unstable circulation modes and an increase in meridional flow75. We observed an association between cooler climate and the levels of fire activity while considered at the decadal through millennia scales (Figs 5 and 6). We speculate that the frequency of fire-prone periods likely increased under cool conditions due to both increased weather instability and the frequency of extreme weather episodes during the generally cooler periods. A study of precipitation variability in Sweden33 has indicated an increased variability at sub-decadal time scales during the LIA. Furthermore, low δ18 Osi values from lakes (suggesting an Arctic provenance of precipitation) have been noted for periods corresponding to low temperature as inferred from tree-ring records35,76. In addition, simulation experiments suggested increased intensity of storms during LIA77. On the annual scales, however, temperature during the fire season did not appear to correlate with annually burned areas in Northern Scandinavia (Fig. SI3).
Charcoal influx in lake sediments in Northern Sweden41, a proxy for regional fire activity, was synchronized with independently reconstructed regional temperature, SST dynamics of the Norwegian and Atlantic sea ice for an interval encompassing most of the Holocene (Fig. 6). Charcoal flux showed an inverse relationship with summer air temperatures reconstructed from diatom and chironomid assemblages in lake sediments37 and with SSTs of the Norwegian Sea. The data suggest higher regional fire activity during phases of NAC weakening and subsequent regional cooling. IRD from the northern North Atlantic50 indicated partial correspondence between paleo fire records41 and sea ice cover extent, which was negatively correlated to SST. In particular, an increase in charcoal flux coincided with an increased amount of sea ice cover in the Labrador Sea52 and IRD in the northern North Atlantic at 7000–8000 and 5000–6000 cal. years BP, whereas the 7000–6000 cal years BP interval corresponds to a decline in charcoal flux and minimum sea ice cover extent (Fig. 6). After 5000 cal years BP, the algorithm failed to detect periods with significantly different levels of IRD. The factors behind the loss of synchronicity between IRD and charcoal flux after 5000 cal. years BP remain unclear. However, we note that geographically closer estimates of climate variability such as August SAT reconstruction in northern Scandinavia and SST records from the Norwegian Sea, consistently exhibited a close correspondence with fire activity as inferred from lacustrine charcoal flux. Direct comparison between the lacustrine isotope record and the North Atlantic IRD also shows a good correspondence but mostly since about 2000 years35.
The proximity of cold and dry Arctic air masses makes the northern Scandinavian forests sensitive to climate variability. Because the southward expansion of Arctic air masses is largely controlled by the North Atlantic SSTs through the shift of westerly storm tracks, one should expect stronger teleconnections between ocean and fire activity in Northern Scandinavia than in more southerly located parts of the European sub-continent. Indeed, numerical experiments have revealed amplified differences in precipitation over Northern Europe from strong to weak AMOC78. This is consistent with the limited synchronicity of Holocene fire activity in northern41 vs. southern Scandinavia79 and with the different patterns of annual fire activity evidenced from both dendrochronological reconstructions28 and 20th century observational data13.
We propose that cold conditions over the northern North Atlantic, associated with low SSTs, redirect southward the precipitation associated with the westerlies and result in increased regional fire activity. Our study demonstrated a previously undocumented teleconnection between the dynamics of Atlantic Ocean and the regional fire activity in northern Europe. The consistency of results obtained from modern observations, dendrochronological, paleolimnological and paleoceanographical reconstructions suggests that teleconnection between North Atlantic SST and fire activity operated on multiple temporal scales during the Holocene, which is relevant for understanding future fire activity in Northern Europe. Two features of the regional climate likely divert fire activity from the a pattern of increasing with temperature. These are: (a) the dominating effect of precipitation on fire activity (Fig. SI 3C) and (b) the decoupling between SAT and precipitation (Fig. SI 3E) that results in fire activity mostly responding to precipitation and atmospheric humidity (Fig. SI 3D).
The link between SST and fire activity in Northern Scandinavia exemplifies a fundamental control of oceanic circulation on natural disturbance regimes in terrestrial ecosystems, as already demonstrated in other regions of the globe. Periods with large wildfires in boreal Canada and Alaska have been linked to the Pacific Decadal Oscillation (PDO), El Nino Southern Oscillation (ENSO)26,80,81 and global SST during the northern hemisphere winter24. In particular, the warmer phases of PDO have been shown to result in increased fire activity over the North American boreal forest. In Patagonia, years of increased fire hazard have been shown to relate to lower SST (La Niña events) leading to heavily reduced precipitation during winter and spring periods82. In Europe, no previous studies have examined the link between Atlantic SST and fire activity, although the predictability of European weather from ocean dynamics has been documented earlier83,84,85.
How to cite this article: Drobyshev, I. et al. Atlantic SSTs control regime shifts in forest fire activity of Northern Scandinavia. Sci. Rep. 6, 22532; doi: 10.1038/srep22532 (2016).
Bond-Lamberty, B., Peckham, S. D., Ahl, D. E. & Gower, S. T. Fire as the dominant driver of central Canadian boreal forest carbon balance. Nature (London) 450, 89–92, doi: 10.1038/nature06272 (2007).
Bowman, D. M. et al. Forest fire management, climate change and the risk of catastrophic carbon losses. Front. Ecol. Environ. 11, 66–68, doi: 10.1890/13.WB.005 (2013).
Amiro, B. D. et al. Fire weather index system components for large fires in the Canadian boreal forest. Int. J. Wildland Fire 13, 391–400, doi: 10.1071/WF03066 (2004).
de Groot, W. J. et al. A comparison of Canadian and Russian boreal forest fire regimes. Forest Ecol. Manag. 294, 23–34, doi: 10.1016/j.foreco.2012.07.033 (2013).
van der Werf, G. et al. Global fire emissions and the contribution of deforestation, savanna, forest, agricultural and peat fires (1997–2009). Atmos. Chem. Phys. 10, 11707–11735, doi: 10.5194/acp-10-11707-2010 (2010).
Mcrae, D. et al. Variability of fire behavior, fire effects and emissions in Scotch pine forests of Central Siberia. Mitig. adapt. strategies glob. chang . 11, 45–74, doi: 10.1007/s11027-006-1008-4 (2006).
Bergeron, Y., Gauthier, S., Flannigan, M. & Kafka, V. Fire regimes at the transition between mixedwood and coniferous boreal forest in Northwestern Quebec. Ecology 85, 1916–1932, doi: 10.1890/02-0716 (2004).
Stocks, B. J. & Lynham, T. J. Fire in ecosystems of boreal Eurasia (eds. Goldammer, J. G. & Furyaev, V. V. ). 481–494 (Kluwer Academic Publishers, Dordrecht, 1996).
Flannigan, M. D. & Wotton, B. M. Forest fires: behavior and ecological effects . (eds. Johnson, E. A. & Miyanishi, K. ), 315–373 (Academic Press, San Francisco, CA, 2001) doi: 10.1016/B978-012386660-8/50012-X (2001).
Pyne, S. J. World Fire: The Culture of Fire on Earth (University of Washington Press, 1997).
Bradshaw, R. H., Lindbladh, M. & Hannon, G. E. The role of fire in southern Scandinavian forests during the late Holocene. Int. J. Wildland Fire 19, 1040–1049, doi: 10.1071/WF09108 (2010).
Niklasson, M. & Granström, A. Numbers and sizes of fires: Long-term spatially explicit fire history in a Swedish boreal landscape. Ecology 81, 1484–1499, doi: 10.2307/177301 (2000).
Drobyshev, I., Niklasson, M. & Linderholm, H. Forest fire activity in Sweden: Climatic controls and geographical patterns in the 20th century. Agr. Forest Meteorol. 154-155, 174–186, doi: 10.1016/j.agrformet.2011.11.002 (2012).
Birks, C. J. A. & Koc, N. A high-resolution diatom record of late-Quaternary sea-surface temperatures and oceanographic conditions from the eastern Norwegian Sea. Boreas 31, 323–344, doi: 10.1111/j.1502-3885.2002.tb01077.x. (2002).
Talandier, C. et al. Improvements of simulated Western North Atlantic current system and impacts on the AMOC. Ocean Model. 76, 1–19, doi: 10.1016/j.ocemod.2013.12.007 (2014).
Marshall, J., Johnson, H. & Goodman, J. A study of the interaction of the North Atlantic oscillation with ocean circulation. J. Climate 14, 1399–1421, doi: 10.1175/1520-0442(2001)014<1399%3AASOTIO>2.0.CO%3B2 (2001).
Trouet, V., Scourse, J. D. & Raible, C. C. North Atlantic storminess and Atlantic Meridional Overturning Circulation during the last Millennium: Reconciling contradictory proxy records of NAO variability. Glob. Planet. Chang. 84-85, 48–55, doi: 10.1016/j.gloplacha.2011.10.003 (2012).
Pearce, C. et al. Ocean lead at the termination of the Younger Dryas cold spell. Nat. Commun. 4, doi: 10.1038/ncomms2686 (2013).
Sutton, R. T. & Hodson, D. L. R. Atlantic Ocean forcing of North American and European summer climate. Science 309, 115–118, doi: 10.1126/science.1109496 (2005).
Hurrell, J. W. & VanLoon, H. Decadal variations in climate associated with the north Atlantic oscillation. Climatic Change 36, 301–326, doi: 10.1023/A:1005314315270 (1997).
Rogers, J. C. North Atlantic storm track variability and its association to the north Atlantic oscillation and climate variability of northern Europe. J. Climate 10, 1635–1647, doi: 10.1175/1520-0442(1997)010<1635:NASTVA>2.0.CO;2 (1997).
Veblen, T. T., Kitzberger, T. & Donnegan, J. Climatic and human influences on fire regimes in ponderosa pine forests in the Colorado Front Range. Ecol. Appl. 10, 1178–1195, doi: 10.1890/1051-0761(2000)010[1178:CAHIOF]2.0.CO;2 (2000).
Gedalof, Z., Peterson, D. L. & Mantua, N. J. Atmospheric, climatic and ecological controls on extreme wildfire years in the northwestern United States. Ecol. Appl. 15, 154–174, doi: 10.1890/03-5116 (2005).
Skinner, W. R., Shabbar, A., Flannigan, M. D. & Logan, K. Large forest fires in Canada and the relationship to global sea surface temperatures. J. Geophys. Res.-Atmos . 111, doi: 10.1029/2005JD006738 (2006).
Yocom, L. L. et al. El Nino-Southern Oscillation effect on a fire regime in northeastern Mexico has changed over time. Ecology 91, 1660–1671, doi: 10.1890/09-0845.1 (2010).
Shabbar, A., Skinner, W. & Flannigan, M. D. Prediction of seasonal forest fire severity in Canada from large-scale climate patterns. J. Appl. Meteorol. Clim . 50, 785–799, doi: 10.1175/2010JAMC2547.1 (2011).
Margolis, E. Q. & Swetnam, T. W. Historical fire-climate relationships of upper elevation fire regimes in the south-western United States. Int. J. Wildland Fire 22, 588–598, doi: 10.1071/WF12064 (2013).
Drobyshev, I. et al. Multi-century reconstruction of fire activity in Northern European boreal forest suggests differences in regional fire regimes and their sensitivity to climate. J. Ecol. 102, 738–748, doi: 10.1111/1365-2745.12235 (2014).
Raab, B. & Vedin, H. Klimat, sjöar och vattendrag. Sveriges National Atlas. SNA Förlag, Stockholm (1995).
Ahti, T., Hämet-Ahti, L. & Jalas, J. Vegetation zones and their sections in northwestern Europe. Ann. Bot. Fenn. 5, 169–211 (1968).
Drobyshev, I. et al. Reconstruction of a regional drought index in southern Sweden since AD 1750. Holocene 21, 667–679, doi: 10.1177/0959683610391312 (2011).
Seftigen, K., Linderholm, H. W., Drobyshev, I. & Niklasson, M. Reconstructed drought variability in southeastern Sweden since the 1650s. Int. J. Climatol. 33, 2449–2458, doi: 10.1002/joc.3592 (2013).
Seftigen, K., Bjöklund, J. A., Cook, E. R. & Linderholm, H. W. A tree-ring field reconstruction of Fennoscandian summer hydroclimate variability for the last millennium. Clim. Dynam. 1–14, doi: 0.1007/s00382-014-2191-8 (2014).
Andersson, S., Rosqvist, G., Leng, M. J., Wastegard, S. & Blaauw, M. Late Holocene climate change in central Sweden inferred from lacustrine stable isotope data. J. Quaternary Sci. 25, 1305–1316, doi: 10.1002/jqs.1415 (2010).
Rosqvist, G. C. et al. Shifts in precipitation during the last millennium in northern Scandinavia from lacustrine isotope records. Quaternary Sci. Rev. 66, 22–34, doi: 10.1016/j.quascirev.2012.10.030 (2013).
Melvin, T. M., Grudd, H. & Briffa, K. R. Potential bias in ‘updating’ tree-ring chronologies using regional curve standardisation: Re-processing 1500 years of Torneträsk density and ring-width data. Holocene 23, 364–373, doi: 10.1177/0959683612460791 (2013).
Larocque, I. & Hall, R. I. Holocene temperature estimates and chironomid community composition in the Abisko Valley, northern Sweden. Quaternary Sci. Rev. 23, 2453–2465, doi: 10.1016/j.quascirev.2004.04.006 (2004).
Drobyshev, I., Goebel, P. C., Hix, D. M., Corace, R. G. & Semko-Duncan, M. E. Pre- and post-European settlement fire history of red pine dominated forest ecosystems of Seney National Wildlife Refuge, Upper Michigan. Can. J. Forest Res. 38, 2497–2514, doi: 10.1139/X08-082 (2008).
Drobyshev, I., Bergeron, Y., Linderholm, H. W., Granstrom, A. & Niklasson, M. A 700-year record of large fire years in northern Scandinavia shows large variability and increased frequency during the 1800s. J. Quaternary Sci. 30, 211–221, doi: 10.1002/jqs.2765 (2015).
Stocks, B. J. et al. Large forest fires in Canada, 1959-1997. J. Geophys. Res.-Atmos . 107, doi: 10.1029/2001JD000484 (2002).
Carcaillet, C., Bergman, I., Delorme, S., Hornberg, G. & Zackrisson, O. Long-term fire frequency not linked to prehistoric occupations in northern Swedish boreal forest. Ecology 88, 465–477, doi: 10.1890/0012-9658(2007)88[465:LFFNLT]2.0.CO;2 (2007).
Blarquez, O. et al. paleofire: An R package to analyse sedimentary charcoal records from the Global Charcoal Database to reconstruct past biomass burning. Comput. Geosci. 72, 255–261, doi: 10.1016/j.cageo.2014.07.020 (2014).
Cavalieri, D. J., Parkinson, C. L., Gloersen, P. & Zwally, H. Sea ice concentrations from Nimbus-7 SMMR and DMSP SSM/I-SSMIS passive microwave data. http://nsidc.org/data/nsidc-0051.html. Date of access 2015-11-12. NSIDC DAAC: NASA DAAC at the National Snow and Ice Data Center. Boulder, Colorado USA (2015).
Rayner, N. A. et al. Global analyses of sea surface temperature, sea ice and night marine air temperature since the late nineteenth century. J. Geophys. Res.-Atmos . 108, doi: 10.1029/2002JD002670 (2003).
Kistler, R. et al. The NCEP-NCAR 50-year reanalysis: Monthly means CD-ROM and documentation. B. Am. Meteorol. Soc. 82, 247–267, doi: 10.1175/1520-0477(2001)082<0247:TNNYRM>2.3.CO;2 (2001).
Saha, S. et al. The NCEP Climate Forecast System Reanalysis. B. Am. Meteorol. Soc. 91, 1015–1057, doi: 10.1175/2010BAMS3001.1 (2010).
Dai, A. G. Characteristics and trends in various forms of the Palmer Drought Severity Index during 1900-2008. J. Geophys. Res.-Atmos . 116, doi: 10.1029/2010JD015541 (2011).
Harris, I., Jones, P. D., Osborn, T. J. & Lister, D. H. Updated high-resolution grids of monthly climatic observations - the CRU TS3.10 Dataset. Int. J. Climatol. 34, 623–642, doi: 10.1002/joc.3711 (2014).
Calvo, E., Grimalt, J. O. & Jansen, E. High resolution U(37)(K) sea surface temperature reconstruction in the Norwegian Sea during the Holocene. Quaternary Sci. Rev. 21, 1385–1394 doi: 10.1016/S0277-3791(01)00096-8 (2002).
Bond, G. et al. Persistent solar influence on north Atlantic climate during the Holocene. Science 294, 2130–2136, doi: 10.1126/science.1065680 (2001).
de Vernal, A. et al. Dinoflagellate cyst assemblages as tracers of sea-surface conditions in the northern North Atlantic, Arctic and sub-Arctic seas: the new ‘n=677’ data base and its application for quantitative palaeoceanographic reconstruction. J. Quaternary Sci. 16, 681–698, doi: 10.1002/jqs.659 (2001).
de Vernal, A. et al. Dinocyst-based reconstructions of sea ice cover concentration during the Holocene in the Arctic Ocean, the northern North Atlantic Ocean and its adjacent seas. Quaternary Sci. Rev. 79, 111–121, doi: 10.1016/j.quascirev.2013.07.006 (2013).
Trouet, V. & van Oldenborgh, G. J. KNMI Climate Explorer: A web-based research tool for high-resolution paleoclimatology. Tree-Ring Res. 69, 3–13, doi: 10.3959/1536-1098-69.1.3 (2013).
Wilks, D. S. On “field significance” and the false discovery rate. J. Appl. Meteorol. Clim . 45, 1181–1189, doi: 10.1175/JAM2404.1 (2006).
Swetnam, T. W. & Betancourt, J. L. Fire - Southern Oscillation relations in the Southwestern United States. Science 249, 1017–1020, doi: 10.1126/science.249.4972.1017 (1990).
van Oldenborgh, G. J. & Burgers, G. Searching for decadal variations in ENSO precipitation teleconnections. Geophys. Res. Lett. 32, doi: 10.1029/2005GL023110 (2005).
Kelly, P. M. & Sear, C. B. Climatic impact of explosive volcanic eruptions. Nature 311, 740–743, doi: 10.1038/311740a0 (1984).
Rodionov, S. N. A sequential algorithm for testing climate regime shifts. Geophys. Res. Lett. 31, doi: 10.1029/2004GL019448 (2004).
Rodionov, S. & Overland, J. E. Application of a sequential regime shift detection method to the Bering Sea ecosystem. Ices Journal of Marine Science 62, 328–332, doi: 10.1016/j.icesjms.2005.01.013 (2005).
Rodionov, S. N. Use of prewhitening in climate regime shift detection. Geophys. Res. Lett. 33, doi: 10.1029/2006GL025904 (2006).
Fratantoni, P. S. & McCartney, M. S. Freshwater export from the Labrador current to the North Atlantic current at the tail of the Grand Banks of Newfoundland. Deep-Sea Res. PT II 57, 258–283, doi: 10.1016/j.dsr.2009.11.006 (2010).
Rossby, T. On gyre interactions. Deep-Sea Res. PT II 46, 139–164, doi: 10.1016/S0967-0645(98)00095-2 (1999).
Behrens, E., Biastoch, A. & Boening, C. W. Spurious AMOC trends in global ocean sea-ice models related to subarctic freshwater forcing. Ocean Model. 69, 39–49, doi: 10.1016/j.ocemod.2013.05.004 (2013).
Frankcombe, L. M., von der Heydt, A. & Dijkstra, H. A. North Atlantic multidecadal climate variability: an investigation of dominant time scales and processes. J. Climate 23, 3626–3638, doi: 10.1175/2010JCLI3471.1 (2010).
Saenko, O. A., Weaver, A. J., Robitaille, D. Y. & Flato, G. M. Warming of the subpolar Atlantic triggered by freshwater discharge at the continental boundary. Geophys. Res. Lett. 34, doi: 10.1029/2007GL030674 (2007).
Moffa-Sanchez, P., Hall, I. R., Barker, S., Thornalley, D. J. R. & Yashayaev, I. Surface changes in the eastern Labrador Sea around the onset of the Little Ice Age. Paleoceanography 29, 160–175, doi: 10.1002/2013PA002523 (2014).
Bader, J. et al. A review on Northern Hemisphere sea-ice, storminess and the North Atlantic Oscillation: observations and projected changes. Atmos. Res . 101, 809–834, doi: 10.1016/j.atmosres.2011.04.007 (2011).
Rosqvist, G., Jonsson, C., Yam, R., Karlen, W. & Shemesh, A. Diatom oxygen isotopes in pro-glacial lake sediments from northern Sweden: a 5000 year record of atmospheric circulation. Quaternary Sci. Rev. 23, 851–859, doi: 10.1016/j.quascirev.2003.06.009 (2004).
Thornalley, D. J. R., Elderfield, H. & Mccave, I. N. Holocene oscillations in temperature and salinity of the surface subpolar North Atlantic. Nature 457, 711–714, doi: 10.1038/nature07717 (2009).
Andersen, C., Koc, N., Jennings, A. & Andrews, J. T. Nonuniform response of the major surface currents in the Nordic Seas to insolation forcing: Implications for the Holocene climate variability. Paleoceanography 19, doi: 10.1029/2002PA000873 (2004).
Park, W. & Latif, M. Ocean dynamics and the nature of air-sea interactions over the North Atlantic at decadal time scales. J. Climate 18, 982–995, doi: 10.1175/JCLI-3307.1 (2005).
Moffa-Sanchez, P., Born, A., Hall, I. R., Thornalley, D. J. & Barker, S. Solar forcing of North Atlantic surface temperature and salinity over the past millennium. Nat. Geosci. 7, 275–278, doi: 10.1038/ngeo2094 (2014).
Gagen, M. et al. Cloud response to summer temperatures in Fennoscandia over the last thousand years. Geophys. Res. Lett. 38, doi: 10.1029/2010GL046216 (2011).
Bergeron, Y. & Archambault, L. Decreasing frequency of forest fires in the southern boreal zone of Quebec and its relation to global warming since the end of the “Little Ice Age”. Holocene 3, 255–259, doi: 10.1177/095968369300300307 (1993).
Jonsson, C. E. et al. High-resolution diatom delta O-18 records, from the last 150 years, reflecting changes in amount of winter precipitation in two sub-Arctic high-altitude lakes in the Swedish Scandes. J. Quaternary Sci. 25, 918–930, doi: 10.1002/jqs.1372 (2010).
Grudd, H. Tornetrask tree-ring width and density AD 500–2004: a test of climatic sensitivity and a new 1500-year reconstruction of north Fennoscandian summers. Clim. Dynam. 31, 843–857, doi: 10.1007/s00382-007-0358-2 (2008).
Raible, C. C., Yoshimori, M., Stocker, T. F. & Casty, C. Extreme midlatitude cyclones and their implications for precipitation and wind speed extremes in simulations of the Maunder Minimum versus present day conditions. Clim. Dynam. 28, 409–423, doi: 10.1007/s00382-006-0188-7 (2007).
Pohlmann, H., Sienz, F. & Latif, M. Influence of the multidecadal Atlantic meridional overturning circulation variability on European climate. J. Climate 19, 6062–6067, doi: 10.1175/JCLI3941.1 (2006).
Olsson, F. et al. A continuous record of fire covering the last 10,500 calendar years from southern - Sweden The role of climate and human activities. Palaeogeography Palaeoclimatology Palaeoecology 291, 128–141, doi: 10.1016/j.palaeo.2009.07.013 (2010).
Fauria, M. M. & Johnson, E. A. Large-scale climatic patterns control large lightning fire occurrence in Canada and Alaska forest regions. J. Geophys. Res.-Biogeo . 111, doi: 10.1029/2006JG000181 (2006).
Wang, Y. H., Flannigan, M. & Anderson, K. Correlations between forest fires in British Columbia, Canada and sea surface temperature of the Pacific Ocean. Ecol. Model. 221, 122–129, doi: 10.1016/j.ecolmodel.2008.12.007 (2010).
Veblen, T. T., Kitzberger, T., Villalba, R. & Donnegan, J. Fire history in northern Patagonia: The roles of humans and climatic variation. Ecol. Monogr. 69, 47–67, doi: 10.2307/2657194 (1999).
Hertig, E. & Jacobeit, J. Predictability of Mediterranean climate variables from oceanic variability. Part II: Statistical models for monthly precipitation and temperature in the Mediterranean area. Clim. Dynam. 36, 825–843, doi: 10.1007/s00382-010-0821-3 (2011).
Feddersen, H. Predictability of seasonal precipitation in the Nordic region. Tellus A . 55, 385–400, doi: 10.1034/j.1600-0870.2003.00027.x (2003).
Colman, A. & Davey, M. Prediction of summer temperature, rainfall and pressure in Europe from preceding winter North Atlantic ocean temperature. Int. J. Climatol. 19, 513–536, doi: 10.1002/(SICI)1097-0088(199904)19:5<513::AID-JOC370>3.0.CO;2-D (1999).
The study was supported by the the Swedish Research Council FORMAS (grant no. 239-2014-1866 to I.D.). The study was conducted within the framework of the Nordic-Canadian network on forest growth research, which is supported by the Nordic Council of Ministers (grant no. 12262 to I.D.), the Swedish-Canadian network on dynamics of the boreal biome, which is supported by the Swedish Foundation for International Cooperation in Research and Higher Education STINT (grant no. IB2013-5420 to I.D.), NSERC Discovery Development Grant (grand no. DDG-2015-00026 to I.D.) and the international consortium GDRI Cold Forests. We thank Arto Miettinen, Oliver Marchal and Eva Calvo for their help in providing ocean coring data, Olivier Blarquez for comments on using the paleofire package and Geert Jan van Oldenborgh for comments on using KNMI Climate Explorer.
The authors declare no competing financial interests.
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Drobyshev, I., Bergeron, Y., Vernal, A. et al. Atlantic SSTs control regime shifts in forest fire activity of Northern Scandinavia. Sci Rep 6, 22532 (2016). https://doi.org/10.1038/srep22532
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