Abstract
We developed two tree-ring chronologies of teak (Tectona grandis L.f.) from Mae Tuen (462-year, 1555–2016) and Umphang (165-year, 1852–2016) in Tak province, northwestern Thailand. The chronologies were based on 67 and 71 living teak trees, respectively. We used crossdating methods to check and verify the tree-ring width data and tree-ring chronology construction using the ARSTAN program. In this study, the two teak tree-ring chronologies from two different growth areas could not be crossdated. The relationship among these chronologies is, thus, relatively low (r = 0.33, n = 165, p < 0.01). This result shows that the growth of tree-ring structure from two sites can be affected by a variety of non-climatic patterns due to site variation, such as topography, nutrient, light, and internal factors. However, these chronologies have a significant positive correlation with rainfall, during the pre-monsoon season (April to May). As demonstrated by the spatial correlation patterns, these chronologies represent April to May rainfall, which was a limiting factor of teak growth from northwestern Thailand. While the difference in surface temperatures of the Indian Ocean Dipole (IOD) might not be affected by rainfall, its unstable relationship with the El Niño-Southern Oscillation (ENSO) was noted to have occurred.
Highlights
The Asian monsoon system (AMS) is a key variable for global climate change and plays a significant role in large-scale climate variability [1]
AMS is composed of three inter-linked components: Indian summer monsoon (ISM), East Asian summer monsoon (EASM), and Southeast Asian summer monsoon (SASM) [5]
Using the tree-ring chronology of teak (Tectona grandis L.f.) from the Mae Tuen (MT) and UP sites in Tak province, northwestern Thailand, we have developed a 462-year MT chronology (1555–2016) that would be the longest chronology of teak in Thailand
Summary
The Asian monsoon system (AMS) is a key variable for global climate change and plays a significant role in large-scale climate variability [1]. The AMS is primarily driven by convective, radiative, and sensible heat sources/sinks [2,3]. Southwest monsoons are formed due to intense low pressure systems formed over the Tibetan plateau. Northeast monsoons are associated with high pressure cells over the Tibetan and Siberian plateaus. Countries like India, Indonesia, Bangladesh, Myanmar, and Thailand receive most of the annual rainfall during the southwest monsoon season [4]. AMS is composed of three inter-linked components: Indian summer monsoon (ISM), East Asian summer monsoon (EASM), and Southeast Asian summer monsoon (SASM) [5].
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