The article contains an analysis of the influence of cloudiness and atmospheric circulation on the components of radiation balance (Q*) using the example of measurements taken in an extra-urban area of Koniczynka near Toruń (Central Poland) in the years 2011–2018. The average annual value of Q* was 1,818.5 MJ·m⁻² with a maximum of 352.3 MJ·m⁻² in June, and negative values from November to January (December: ⁻27.4 MJ·m⁻²). The shortwave radiation balance (S*) amounted to 3,129.2 MJ·m⁻² and the longwave radiation balance (L*) was ˗1,310.7 MJ·m⁻². In June the average solar irradiance (S↓) at midday was 600 W·m⁻². The natural annual and diurnal course of Q* components, determined by astronomical factors, is disturbed by changes in cloudiness and inflow of various air masses. It has been found that an increase in cloudiness causes the amount of incoming solar radiation (S↓) to fall, thus decreasing the S* balance. Moreover, clouds restrict longwave radiation balance (L*), in particular, downward atmospheric radiation (L↓) increases. The opposite relationships of S* and L* affect Q* in individual months. The components of Q* are influenced by atmospheric circulation; it has been observed that anticyclonic types, characterised by smaller cloud amounts, favour a greater influx of (S↓) and—at the same time—greater emittance (L↑); however, Q* is then greater than in the case of cyclonic circulation. A statistically significant trend of Q* and its components has not been ascertained. A notable great year-on-year variability of Q*, ranging from 1,640.4 MJ·m⁻² (in 2011) to 2,081.6 MJ·m⁻² (in 2018), affects the environment. The changes are related to the cloudiness and the frequency of occurrence of different atmospheric circulation types. The role of snow cover is also important as snow reflects solar radiation which leads to the decrease of S* and—as a result—to a negative value of Q* in winter.

本文以2011-2018年在托伦（波兰中部）附近的Koniczynka郊区地区进行的测量为例，分析了混浊和大气环流对辐射平衡（Q *）成分的影响。Q *的年平均值为1,818.5 MJ·米^-2最多352.3 MJ的·米^-2六月，负值从11至1月（十二月：^- 27.4 MJ·米^-2）。短波辐射平衡（S *）为3,129.2 MJ·m ^-2，长波辐射平衡（L *）为˗1,310.7MJ·m ^-2。6月的中午平均太阳辐照度（S↓）为600 W·m ^-2。由天文因素决定的Q *分量的自然年度和昼夜变化过程，受多云度和各种气团流入的变化的干扰。已经发现，浑浊的增加导致入射的太阳辐射量（S↓）下降，从而降低了S *平衡。此外，云限制了长波辐射平衡（L *），特别是向下的大气辐射（L↓）增加。S *和L *的相反关系会影响各个月的Q *。Q *的成分受大气环流的影响；已经观察到，以云量较小为特征的反气旋类型，有利于（S↓）的大量涌入，同时也具有更大的发射率（L↑）；但是，Q *大于旋风循环的情况。尚未确定Q *及其成分的统计学显着趋势。Q *的显着年度差异很大，范围为1,640.4 MJ·m⁻²（2011年）至2,081.6 MJ·m ⁻²（2018年），会影响环境。这些变化与不同的大气环流类型的浑浊和发生频率有关。积雪的作用也很重要，因为积雪会反射太阳辐射，从而导致S *降低，从而导致冬季的Q *值为负。