ライフサイエンスコーパス: boreal forest

1 hanging climate and atmospheric [CO2] in the boreal forest.

2 vegetation dominance in 100 Mha of Canadian boreal forest.

3 ake in a large portion of the North American boreal forest.

4 est growth when averaged across the Canadian boreal forest.

5 arbon, influenced chlorination of SOM from a boreal forest.

6 orage on land, particularly in temperate and boreal forests.

7 Herein, we demonstrate such a feedback in boreal forests.

8 sing tropical, Mediterranean, temperate, and boreal forests.

9 uency--the primary disturbance agent in most boreal forests.

10 bably underestimated N-fixation potential in boreal forests.

11 emperate forests and losses in some Canadian boreal forests.

12 tion strategies to maintain western Canadian boreal forests.

13 son periods for Alaskan and western Canadian boreal forests.

14 P, increasing with latitude from tropical to boreal forests.

15 larger in warm tropical forests than in cold boreal forests.

16 foundation species in northern temperate and boreal forests.

17 (%N) has been reported in some temperate and boreal forests.

18 along a gradient from temperate to subarctic boreal forest (38 sites between latitudes 48 degrees N a

19 performed a warming experiment in an Alaskan boreal forest and examined changes in the prevalence of

20 already been observed in some North American boreal forests and has been attributed to changes in sit

21 ots include large areas such as the Nearctic boreal forests and tundra that are unrepresented in most

22 he global average, the way in which the vast boreal forests and tundras may respond is poorly underst

23 iterranean forests and taller gymnosperms in boreal forests) and latitudinal gradients (e.g. larger p

24 N-use efficiency is highest in boreal forests, and P-use efficiency in tropical forests

25 moose and elk at about 11.5 cal. kyr bp, and boreal forest approximately 10 cal. kyr bp.

26 re range, these treeless states coexist with boreal forest ( approximately 75% tree cover) and with t

27 most fire-prone areas of the North American boreal forest are resistant to high burn rates because o

28 te warms in New England, USA, high-elevation boreal forests are expected to recede upslope, with nort

29 relationships between k and winter length in boreal forests are not consistent between different regi

30 utbreaks of tularemia in a tularemia-endemic boreal forest area of Sweden and that environmental vari

31 tial association of mosquito prevalence in a boreal forest area with transmission of the bacterial di

32 as a result of forestation in temperate and boreal forest areas, and translate these forcings into e

33 I suggest that in many boreal forest areas, the positive forcing induced by dec

34 hypothesis is that widespread masting in the boreal forest at high latitudes is driven primarily by f

35 riability in the Arctic tundra, parts of the boreal forest belt, the tropical rainforest, alpine regi

36 se study Fischer-Tropsch diesel derived from boreal forest biomass in Finland.

37 ional mode diversification suggests that the boreal forest biome originated via genetic coevolution o

38 one of the most flammable ecoregions of the boreal forest biome, to infer causes and consequences of

39 permafrost degradation is well documented in boreal forests, but the role of fires in initiating ther

40 These results suggest that boreal forests can sustain high-severity fire regimes fo

41 changing environmental conditions on the net boreal forest carbon balance have not taken into account

42 adic permafrost zone of northwestern Canada, boreal forest carbon dioxide (CO2 ) fluxes will be alter

43 ea increased significantly from temperate to boreal forests, coinciding with longer and thinner root

44 ielded 12 other mammals and the remains of a boreal-forest community.

45 s due to climate change may cause a shift in boreal forest composition toward reduced dominance of co

46 Fire is a primary driver of boreal forest dynamics.

47 OS) mining operations has on the surrounding boreal forest ecosystem requires a rigorous approach to

48 Lowland boreal forest ecosystems in Alaska are dominated by wetl

49 red in the location of the northern hardwood-boreal forest ecotone (NBE) from 1964 to 2004.

50 ctivity declines across large regions of the boreal forest, even for trees located in cool and moist

51 rglacial [Marine Isotope Stage (MIS) 5] when boreal forests existed regionally.

52 These results suggest that the impact of boreal forest fire emissions on air quality in the mid-l

53 We report measurements and analysis of a boreal forest fire, integrating the effects of greenhous

54 ts found in-situ immediately after a typical boreal forest fire.

55 ion varied greatly since 1788 as a result of boreal forest fires and industrial activities.

56 veground biomass stem growth across Canada's boreal forests from 1950 to the present.

57 Nitrogen-fixation in northern European boreal forests has been estimated at only 0.5 kg N ha(-1

58 Final harvest (clear-cutting) of coniferous boreal forests has been shown to increase streamwater co

59 ar, recent site-level studies of the Alaskan boreal forest have reported both increases and decreases

60 forests and an increased aspen mortality in boreal forests have been associated with global warming,

61 ing in winter with net cooling annually; and boreal forests have strong warming in winter and moderat

62 This study emphasizes the importance of boreal forest humus soils for Hg storage and reveals tha

63 The boreal forests, identified as a critical "tipping elemen

64 quence spanning over more than 5000 years in boreal forest in northern Sweden that belowground invent

65 ss multiple plots in four field sites within boreal forest in the discontinuous permafrost zone (NWT,

66 e high frequency of wildfire disturbances in boreal forests in China, the effects of wildfires on soi

67 f fire on insect diversity from northern and boreal forests in North America.

68 s from 16,450 stands across 583,000 km(2) of boreal forests in Quebec, Canada, we observe a latitudin

69 Increased permafrost thaw in lowland boreal forests in response to warming may have consequen

70 Wildfire activity in North American boreal forests increased during the last decades of the

71 h evaporative cooling, but the low albedo of boreal forests is a positive climate forcing.

72 Wildfire activity in boreal forests is anticipated to increase dramatically,

73 primary successional forests, N-fixation in boreal forests is considered to be extremely limited.

74 position in the Alaskan and western Canadian boreal forests is projected to shift toward early-succes

75 rn extratropical land ecosystems, focused on boreal forests, is implicated, substantially more than s

76 ses from reservoirs constructed on an upland boreal forest landscape in order to quantify their depen

77 Boreal forest loss due largely to fire and forestry was

78 rmafrost zone of North America, thaw-induced boreal forest loss is leading to permafrost-free wetland

79 Therefore, permafrost thaw-induced boreal forest loss may modify regional precipitation pat

80 emote sensing to characterize the impacts of boreal forest loss on albedo, eco-physiological and aero

81 g has led to increased productivity near the boreal forest margin in Alaska.

82 arbon sink, suggesting that western Canada's boreal forests may become net carbon sources if the clim

83 within natural ecosystems, yet the origin of boreal forest N has remained elusive.

84 tral and western portions of the continent's boreal forest, northeastern North America may act as a c

85 ight the prominence of drought stress in the boreal forest of interior Alaska.

86 esponse to climate warming and drying in the boreal forest of interior Alaska.

87 erity and environmental factors post-fire in boreal forests of China.

88 The boreal forests of Eurasia and North America lack any sig

89 ase in water-use efficiency in temperate and boreal forests of the Northern Hemisphere over the past

90 Boreal forests play critical roles in global carbon, wat

91 al Forest, NH, and suggest that processes of boreal forest recovery from prior red spruce decline, or

92 er enables more comprehensive assessments of boreal forest recovery.

93 High C partitioning belowground in boreal forests reflects a 13-fold greater C cost of N ac

94 es, and turbulent energy fluxes of a lowland boreal forest region in the Northwest Territories, Canad

95 al N is unacceptable given the extent of the boreal forest region, but predictable given our imperfec

96 Young boreal forests represent a relatively small but persiste

97 ew particle formation events at the Hyytiala boreal forest research station.

98 ha for tropical, subtropical, temperate, and boreal forests, respectively.

99 ind that net ecosystem CO2 uptake (NEE) in a boreal forest rose linearly by 4.7 +/- 0.2% of the curre

100 ystem CO(2) uptake capacity in temperate and boreal forests scales directly with whole-canopy N conce

101 The data reveal that boreal forest shows no gradual decline in tree cover tow

102 amples collected over a two week period at a boreal forest site (Hyytiala), southern Finland.

103 Across 35 temperate and boreal forest sites with field N-fertilization experimen

104 able isotope signatures of radiocarbon-dated boreal forest soils and modeled atmospheric Hg depositio

105 Our data clearly show that northern boreal forest soils have a strong sink capacity for Hg,

106 37)Cl in bulk organochlorines extracted from boreal forest soils were only slightly depleted in (37)C

107 Empirical evidence from the Alaska boreal forest suggests that every 1% reduction in overal

108 carbon uptake in high latitudes and for the boreal forest system as a whole.

109 In boreal forests, the combined effects of recent warming a

110 s are expected to disrupt the functioning of boreal forests, their ultimate implications for forest c

111 y ago), following the ecological shift from boreal forest to steppe tundra.

112 lands may decrease the fluxes of metals from boreal forests to downstream recipients by up to 40% at

113 egatively affect the photosynthetic rates of boreal forest tree saplings at their southern range limi

114 n sink of natural stands throughout Canada's boreal forests using data from long-term forest permanen

115 nce of an open-air warming experiment called Boreal Forest Warming at an Ecotone in Danger (B4WarmED)

116 s balsamea saplings growing in the B4Warmed (Boreal Forest Warming at an Ecotone in Danger) experimen

117 r this signal is present across the northern boreal forest, we compiled published carbon isotope data

118 consequences of intensifying fire regimes in boreal forests, we studied postfire regeneration in five

119 creased through the climatic transition when boreal forests were locally extirpated.

120 large regional increases across much of the boreal forest, western Amazonia, central Africa, western

121 thaw-induced increase in CH4 emissions for a boreal forest-wetland landscape in the southern Taiga Pl

122 temperature- and light-limited NEELAND of a boreal forest-wetland landscape.

123 pparent carbon accumulation rates in similar boreal forest-wetland landscapes and eddy covariance lan

124 n without moisture stress, net CO2 uptake of boreal forest-wetland landscapes may decline, and ultima

125 monstrate that a conversion of a present-day boreal forest-wetland to a hypothetical homogeneous wetl

126 es, but are consistently more pronounced for boreal forests where carbon fluxes are smaller.

127 s hardwood cover are similar among different boreal forests, which differ in the ecological traits of

128 ave been occurring for decades in the global boreal forest, with future climate change likely to incr