本研究分析採自貴州(華南)晚古生代納水剖面、羅悃剖面、納嬈剖面1134個碳酸鹽岩標本的碳、氧穩定同位素成份，以探討同一海盆但不同地點、不同沉積環境間進行碳同位素地層的比對，並用以探討其意義重建古環境。
根據牙形刺生物地層，納水剖面年代包括中石炭紀、中二疊紀；羅悃剖面年代涵蓋中、晚石炭紀；納嬈剖面所涵蓋的年代為中石炭紀到中二疊紀。納水剖面，δ18O數值介於-13.3~-1.1‰ (平均值為-5.6±2.4‰，N=246)； δ13C數值介於-1.1~5.5‰ (平均值為3.2±1.3‰，N=246)。羅悃剖面，δ18O數值介於-9.7~-1.4‰ (平均值為-5.2±1.7‰，N=191)；δ13C數值介於-3.0~5.0‰ (平均值為2.3±1.4‰，N=191)。納嬈剖面，δ18O數值介於-12.9~3.8‰ (平均值為-4.6±1.7‰，N=583)；δ13C數值介於-0.4~6.4‰ (平均值為3.6±1.2‰，N=583)。
研究結果顯示深色碳酸鹽岩(深水相)較其他淺色碳酸鹽岩(淺水相)的碳、氧同位素數值分別重0~2‰、0.1~4.5‰；相較於深水相的沉積環境，淺水相碳酸鹽岩的碳同位素組成變化幅度較大；因此，推論沉積環境的不同或者改變，會造成碳同位素地層對比上組成變化幅度的落差，但整體變化趨勢是一樣的。
在本研究與中國、全球的碳同位素紀錄變化趨勢與幅度大致相同，平均δ13C數值從Visean和Serpukhovian的2~3‰開始增加，在Gzhelian - Asselian之間，δ13C數值達到最大值，為一個明顯的正偏移事件，造成此δ13C正偏移事件，可能與在Gzhelian–Asselian冰川範圍達到最大程度有關。二疊紀，中國華南與北美洲同時Asselian開始δ13C數值往負偏移，是由於冰期開始萎縮所造成的。在Kungurian時期中國華南與北美洲的δ13C數值都有先往負偏移再往正偏移的變化，而正偏移時與Fielding等人(2008)認為冰期發展時的時間相近，顯示此正偏移與冰期有關，但低緯度與Urals的δ13C數值變化趨勢則剛好相反。在Roadian、Wordian、Capitanian時期中國華南、低緯度地區與北美洲的δ13C數值正偏移與冰期發育的時期一致。
本研究結果顯示不論是深水相或淺水相的碳酸鹽岩，其碳酸鹽碳穩定同位素分析值的正偏移，都可以對比其他地區的，應可反映有機碳的大量埋藏、冰川的擴張或縮減，並且可以用來作為輔佐地層對比的工具。

Stable carbon and oxygen isotope compositions of 1,134 carbonate rock samples, collected from Late Paleozoic Nashui section, Luokun section and Narao section, Guizhou (South China) were analyzed to explore the possibility of stratigraphic correlation using carbon isotope records and to estimate the extent of the variation in isotope records between shallow water and deep water environments of the same basin.
Conodont biostratigraphy data was provided by Nanjing Institute of Geology and Palaeontology. Average stable carbon and oxygen isotope of Nashui section (N = 246; middle Carboniferous and middle Permian) are 3.2±1.3‰ and -5.6±2.4‰, respectively. Average stable carbon and oxygen isotope of Luokun section (N = 191; middle to late Carboniferous) are 2.3±1.4‰ and -5.2±1.7‰, respectively. Average stable carbon and oxygen isotope of Narao section (N = 583; middle Carboniferous to Permian) are 3.6±1.2‰ and -4.6±1.7‰, respectively. Carbon and oxygen isotope values of dark- colored carbonates (deep-water) are greater than those of light-colored carbonate rocks (shallow water) 0 ~ 2 ‰ and 0.1 ~ 4.5 ‰, respectively.
Trends and magnitude of the carbon isotope stratigraphy among this study and those of China, North America, and Europe are comparable. Mean δ13C value increases from 2 ~ 3 ‰ during the Visean and Serpukhovian to Gzhelian – Asselian boundary, reaches the maximum. This positive δ13C excursion may be related to the expansion of continental ice volume. In Permian, the δ13C value declined during the Asselian in the South China and North America, potentially coincided with the shrinking of the Carboniferous – Permian ice sheet. In Kungurian period δ13C values of the South China and North America decreased first then increased again. This positive excursion may also be related to the development of ice volume. However, δ13C record at low latitudes (Urals) was opposite to those of South China and North America for Kungurian. In the Roadian, Wordian, Capitanian, δ13C values positive excursion of this study, consisted with the glacial record, coincided with δ13C records of South China, low latitudes, and North America.
This study shows that carbonate rock stable carbon isotope stratigraphy records can be used for stratigraphic correlation with biostratigraphic controls. Positive excursion of δ13C records from both deep water and shallow water sections can be correlated globally and are consistent with the ice volume records.

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