热带次生林林窗不同热力作用面特征分析

利用热带次生林林窗边缘树表温和林窗区域地表温的观测资料,探讨了昼间林窗各热力作用面的热力效应及其变化规律,通过分析林窗边缘树表温和林窗地表温的变化,指出在林窗区域林窗边缘墙面是林冠面,林窗地面,林内地面之外的亲的第4热力作用面;各个热力作用面的热力效应随季节,位置和时刻的不同有着明显差异,在受浓雾影响的上午,林窗地面热力作用较强,在中午和下午林窗东侧林缘壁面,林窗东侧－东北侧地面的热力作用显著,中乖以林窗地面作用较强;而下午则以林窄边缘墙面作用较强,各个较力作用面的热力特征和相互作用将制约林窗的热力变化,影响植物的生长。     

热带季节雨林林窗边缘不同热力作用面热力效应的季节变化特征

通过对热带季节雨林雾凉季和湿热季昼间林窗区域不同热力作用面的热力效应初步分析,指出在西双版纳,不论是雾凉季还是湿热季,热带季节雨林林窗边缘壁面均具有不可忽视的热力作用,且由于受林缘树木的影响,热力效应较强的东侧,北侧林缘壁面最大区域出现位置高于次生林林窗,而强度小于次生林林窗,显示了林窗边缘壁面的热力效应除与太阳高度角,太阳辐射的时间长短和强度有关之外,林窗边缘树木高度也是不可忽视的因子,其结果可为进一步研究林窗小气候形成机制提供研究基础,为研究林窗更新及生物多样性问题提供科学参考。     

哀牢山亚热带常绿阔叶林乔木碳储量及固碳增量

为了解哀牢山亚热带常绿阔叶林的乔木碳储量及其固碳增量,利用2005和2008年的植被调查数据,对哀牢山3种主要常绿阔叶林的乔木碳储量及其固碳增量进行了分析。结果表明:原生的中山湿性常绿阔叶林、滇山杨次生林和旱冬瓜次生林的乔木碳储量分别为257.90、222.95和105.39tC·hm-2;中山湿性常绿阔叶林乔木碳储量主要存储在DBH≥91cm的乔木中(34.68%);而次生林的乔木碳储量主要分布在径级21cm≤DBH41cm的乔木中(滇山杨林77.29%;旱冬瓜林69.28%)。由此可见,哀牢山地区原生的中山湿性常绿阔叶林乔木层在碳蓄积方面占主导优势。哀牢山亚热带常绿阔叶林的3个森林类型乔木层均具有固碳增量,即使是原生的中山湿性常绿阔叶林,其乔木层年平均固碳增量也达2.47tC·hm-2·a-1;次生林乔木层的年平均固碳增量约为原生林的2倍,显示了哀牢山亚热带常绿阔叶林乔木层具有较强的碳汇增量。初步估算,哀牢山亚热带常绿阔叶林林区内每年乔木固碳增量为8.52×104tC·a-1。     

哀牢山常绿阔叶林鸟类群落初步分析

常绿阔叶林是云南境内重要的自然资源,也是我国亚热带地区最主要的原生植被类型。是森林生态系统的主要研究对象之一。鸟类是森林生态系统的重要组分,为便于自然保护区的规划、管理及对鸟类资源的保护和研究,本文报道有关哀牢山常绿阔叶林鸟类群落动态。 自然环境和工作概况     

中国热带静风区林缘水平热力特征的初步分析

利用我国热静风区－西双版纳橡胶林西南向边缘１月的温度观测资料,探讨了昼间林缘区域热力特征及时空变化规律,结果表明,在林缘存在着明显的热力效应;对地面温度的影响深度可至林内约１３ｍ处,地面温度在林处４．５ｍ处达最高,气温则在林缘（０ｍ）出现最大;林缘附近热量的输送在数值和方向上存在较大差异,即林外热量从地面向空中输送;林内在午后与林外相反,热量由上（林冠）向下（地面）输送;林缘附近则在不同地点、不同     

哀牢山亚热带常绿阔叶林内外地温分布特征

地温是森林气候重要的环境因素之一,与植物生长密切相关,对地温的深入研究有助于揭示森林生态系统功能和评估森林环境效益。本文利用哀牢山亚热带常绿阔叶林林内和林外旷地(气象站)地温数据,分析发现:哀牢山亚热带常绿阔叶林林内外的地温均呈单峰型日变化,与林外相比,林内地温具有明显日变化的深度较浅(仅在20cm深度以上);林内平均地温具有显著日变化的深度在春季和秋季(20cm)要大于夏季和冬季(15cm);与林外相比,林内各层地温均小于同层的林外地温,并且林内地温的日变幅和年变幅也小于同深度的林外地温。总体来看,林外地温的年变幅和日变幅大于林内。     

西双版纳热带次生林林窗小气候要素的时空分布特征

利用西双版纳雾凉季和干热季热带次生林林窗的小气候垂直观测资料,探讨了昼间林窗区域树表温、气温、水汽压及相对湿度的时空分布和变化规律,指出在林窗区域,林窗边缘不仅具有显著的热力效应,同样具有明显的水汽效应。并由此构成了林窗区域立体空间的环境异质性,其结果对深入探讨林窗区域的热量、水汽传输,小气候的形成机制,生物多样性和更新等问题均具有重要意义。利用西双版纳雾凉季和干热季热带次生林林窗的小气候垂直观测资料,探讨了昼间林窗区域树表温、气温、水汽压及相对湿度的时空分布和变化规律,指出在林窗区域,林窗边缘不仅具有显著的热力效应,同样具有明显的水汽效应。并由此构成了林窗区域立体空间的环境异质性,其结果对深入探讨林窗区域的热量、水汽传输,小气候的形成机制,生物多样性和更新等问题均具有重要意义。     

西双版纳热带雨林和哀牢山亚热带常绿阔叶林雾特征研究

以西双版纳热带雨林和哀牢山亚热带常绿阔叶林为研究对象,利用PWS100天气现象仪获取两种森林类型的能见度数据。基于2014年西双版纳热带雨林和哀牢山亚热带常绿阔叶林的能见度数据,对两种森林类型雾的特征进行定量研究。研究结果表明:(1)西双版纳热带雨林全年雾日数为196 d,占全年的53.7%,哀牢山亚热带常绿阔叶林全年雾日数为100 d,占全年的27.4%,热带雨林全年雾日数几乎为亚热带常绿阔叶林雾日数的两倍;(2)热带雨林雨季和干季各占28.06%和71.94%,而亚热带常绿阔叶林雨季和干季各占72%和28%;(3)热带雨林一日内雾持续的最长时间为10.5 h,而亚热带常绿阔叶林雾生成和消散时间不定,一日内雾最长持续时间可达24 h,但雾发生的频率低于西双版纳热带雨林。两种森林类型全年雾日特征有明显的差异性,通过定量评价地处过渡带上的两种多雾森林生态系统雾特征,可为未来气候变化对不同森林生态系统碳水交换影响提供数据支撑。     

哀牢山亚热带常绿阔叶林土壤含水量变化规律及其影响因子

利用ChinaFlux设置在哀牢山亚热带常绿阔叶林内的通量观测系统的土壤含水量数据,分析了哀牢山亚热带常绿阔叶林内土壤含水量的时间变化及其影响因子,以期了解哀牢山亚热带常绿阔叶林土壤含水量特征及其变化规律,为森林固碳能力、潜力和速率研究提供支撑.结果表明:(1)哀牢山亚热带常绿阔叶林不同深度土壤含水量大致呈单峰曲线分布,各层土壤含水量基本上随着土壤深度的增加而降低,波动范围也逐渐减小,最小值均在3月,最大值集中在7、8、9三个月.(2)0 ～ 100 cm各层深度的土壤含水量在17.7％～39.5％波动,其中100 cm深度的土壤含水量值最低、波动范围最小,总体来看,土壤含水量雨季高于旱季.(3)土壤含水量主要受降雨量、地温和相对湿度等要素的影响(P＜0.05),哀牢山亚热带常绿阔叶林5 cm深度的土壤含水量最大,约为38％.     

亚热带常绿阔叶林若干树种分布与Penman指标关系的探讨

根据中国亚热带常绿阔叶林区域的气象资料和植物分布资料,计算了组成中国亚热带常绿阔叶林１４个主要科１１２个优势种及常见种的Ｐｅｎｍａｎ可能蒸散（ＰＥ）值和干燥度（Ａ）值,按气候指标的分布范围将优势种和常见种划分为５个水热分布类群,分别为：Ｇ１低温湿润型,Ｇ２低温半湿润型,Ｇ３中温湿润型,Ｇ４中温半湿润型,Ｇ５高温湿润型,并分析其生态气候特征,所得结果较好表现了中国亚热带常绿阔叶林主要树种沿水热梯度的分布格局。虽然Ｐｅｎｍａｎ指标的计算比较复杂,但因其坚实的物理学基础而应用较广,对常绿阔叶林树种与气候关系的研究有一定的参考价值。     

缙云山片断常绿阔叶林小气候边缘效应的初步研究

对缙云山5个片断常绿阔叶林和1个连续常绿阔叶林林缘附近的小气候要素水平梯度分布进行测定.结果表明,各片断阔叶林斑块边缘均存在明显的小气候边缘效应.林缘与林内最高和最低气温、光合有效辐射、最小相对湿度均为干季高于或大于雨季,而地表最高温度则为雨季高于干季;各阔叶林斑块的小气候边缘效应以最大斑块波及林内的深度最浅、最小斑块波及林内的深度最深.     

植被覆盖度和归一化湿度指数对热力景观格局的影响——以广州为例

利用LANDSAT-5 TM影像提取地表温度、植被覆盖度和归一化湿度指数(NDMI)等信息,结合景观生态学方法探讨广州市不同区域城市植被和NDMI对地表温度的调节作用.结果表明:植被覆盖度、NDMI和地表温度两两之间有较强的线性相关性,但不同区域植被覆盖度、NDMI与地表温度的相关程度存在明显差异;提高相同植被覆盖度时,中心城区的降温效果最好,其次是处于中心城区北缘的近郊区;不同区域森林公园对周围热环境的影响程度不同,960～1080 m缓冲区内平均温度与公园内部平均温度之差分别为4.69℃(白云山)、1.27℃(马仔山)和0.41℃(流溪河);高植被覆盖度可增加热力景观多样性和不同景观之间的结合度,促进低温斑块内部与其他斑块如高温斑块间的能量交换,起到控制热岛效应的效果;增加环境湿度与提高植被覆盖度对热力景观格局所形成的作用相当.     

植被覆盖度和归一化湿度指数对热力景观格局的影响——以广州为例

利用LANDSAT-5 TM影像提取地表温度、植被覆盖度和归一化湿度指数（NDMI）等信息,结合景观生态学方法探讨广州市不同区域城市植被和NDMI对地表温度的调节作用.结果表明： 植被覆盖度、NDMI和地表温度两两之间有较强的线性相关性,但不同区域植被覆盖度、NDMI与地表温度的相关程度存在明显差异;提高相同植被覆盖度时,中心城区的降温效果最好,其次是处于中心城区北缘的近郊区;不同区域森林公园对周围热环境的影响程度不同,960~1080 m缓冲区内平均温度与公园内部平均温度之差分别为4.69 ℃（白云山）、1.27 ℃（马仔山）和0.41 ℃（流溪河）;高植被覆盖度可增加热力景观多样性和不同景观之间的结合度,促进低温斑块内部与其他斑块如高温斑块间的能量交换,起到控制热岛效应的效果;增加环境湿度与提高植被覆盖度对热力景观格局所形成的作用相当.     

Does forest fragmentation cause an increase in forest temperature?

Forest fragmentation is considered by many to be a primary cause of the current biodiversity crisis. The underlying mechanisms are poorly known, but a potentially important one is associated with altered thermal conditions within the remaining forest patches, especially at forest edges. Yet, large uncertainty remains about the effect of fragmentation on forest temperature, as it is unclear whether temperature decreases from forest edge to forest interior, and whether this local gradient scales up to an effect of fragmentation (landscape attribute) on temperature. We calculated the effect size (correlation coefficient) of distance from forest edge on air temperature, and tested for differences among forest types surrounded by different matrices using meta-analysis techniques. We found a negative edge-interior temperature gradient, but correlation coefficients were highly variable, and significant only for temperate and tropical forests surrounded by a highly contrasting open matrix. Nevertheless, it is unclear if these local-scale changes in temperature can be scaled up to an effect of fragmentation on temperature. Although it may be valid when considering “fragmentation” as forest loss only, the landscape-scale inference is not so clear when we consider the second aspect of fragmentation, where a given amount of forest is divided into a large number of small patches (fragmentation per se). Therefore, care is needed when assuming that fragmentation changes forest temperature, as thermal changes at forest edges depend on forest type and matrix composition, and it is still uncertain if this local gradient can be scaled up to the landscape.     

Edge Effects of Linear Canopy Openings on Tropical Rain Forest Understory Microclimate

We investigated microclimatic edge gradients associated with grassy powerlines, paved highways and perennial creeks in wet tropical forest in northeastern Australia during wet and dry seasons. Photosynthetically active radiation, air temperature and vapor pressure deficit, soil temperature, canopy temperature, soil moisture, and air speed in the rain forest understory were measured during traverses perpendicular to the forest edge. Light intensity was elevated near the edges of powerlines, highways, and creeks, but this effect was strongest for creek edges. Air temperature and vapor pressure deficit were elevated near powerline edges in the dry season and highway edges in both wet and dry seasons but were not elevated near creek edges in either season. In contrast, soil moisture was lowered near creek edges but not near either powerline or highway edges. No edge gradients were detected for air speed. Canopy temperature was elevated near highway edges and lowered near powerline edges in the wet season but no edge gradients in canopy temperature were detected near creek edges in either the wet or the dry season. We suggest that these different edge gradients may be largely the result of differences in the fluxes of latent and sensible heat within each type of linear canopy opening, with periodic flood disturbance assisting by maintaining a more open canopy near creek edges. Our data indicate that the nature of the linear canopy opening is at least as important as the width in determining the nature and severity of microclimatic edge effects, analogous to the "matrix effect" of traditional fragmentation studies.     

Density structure of the fine surface water layer of large lakes and remote measurement of the temperature

Remote sensing of surface temperatures in large lakes differs in some critical respects from that in marine conditions. Firstly, the atmospheric structure over large lakes has some continental features, which makes the calculation of its influence more complicated. Secondly, the vertical temperature structure in the fine surface layer of a lake is more complex than in marine waters. A prominent feature of the thermal structure of spring heating of large lakes (e.g. in Lake Ladoga from May to July) is the existence of a thermal front, which is manifested on the lake surface as a fine strip with steep horizontal temperature gradient. The existence of a thermal front makes it possible to calibrate infra-red space survey data without using in situ surface temperature measurements. The calibration of arbitrary heat brightness values for +4 °C can be obtained by plotting a frequency distribution histogram of the heat brightness values obtained for the IR-image pixels. While the thermal front is in existence, the heat brightness frequency distribution appears bimodal, and the brightness value at the minimum between the peaks is assigned the temperature of +4 °C. Laboratory and field experiments have enabled us to separate two types of near-surface density structures. Under conditions of density instability in the fine surface layer, microconvection limits the magnitude of vertical temperature difference in this layer to a constant range of 0.6–0.8 °C. However, when a stable density structure prevails during calm conditions, much greater vertical temperature differences may exist.