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© 2018 Geological Society of America. For permission to copy, contact [email protected]. Published online XX Month 2018

An ~34 m.y. astronomical time scale for the uppermost Mississippian through Pennsylvanian of the Carboniferous System of the Paleo-Tethyan realm Huaichun Wu1,2,*, Qiang Fang1,2, Xiangdong Wang3,4, Linda A. Hinnov5, Yuping Qi4, Shu-zhong Shen3,4, Tianshui Yang1, Haiyan Li1, Jitao Chen4, and Shihong Zhang1 1State Key Laboratory of Biogeology and Environmental Geology, China University of Geosciences, Beijing 100083, China 2School of Ocean Sciences, China University of Geosciences, Beijing 100083, China 3Centre for Research and Education on Biological Evolution and Environment, Nanjing University, Nanjing 210023, China 4State Key Laboratory of Palaeobiology and Stratigraphy, Nanjing Institute of Geology and Palaeontology and Center for Excellence in Life and Paleoenvironment, Chinese Academy of Sciences, Nanjing 210008, China 5Department of Atmospheric, Oceanic, and Earth Sciences, George Mason University, Fairfax, Virginia 22030, USA ABSTRACT Time Scale 2016 (GTS2016; Ogg et al., 2016). However, the inferred The Naqing section in South China is a representative carbonate Carboniferous chronostratigraphic framework needs further improve- slope succession in the eastern Paleo-Tethyan realm. It encompasses ment, because: (1) the pan-Euramerican framework cannot be applied at a four global stratotype section and point (GSSP) candidates for the Car- global scale through conodont or fusulinid biozone correlation due to bio- boniferous Period. High-resolution magnetic susceptibility measure- diachronism and provincialism (Davydov et al., 2012); (2) astronomically ments through the section have variations that correlate with lithologi- forced sedimentary cycles from other continents are required to affirm cal cycles of lime mudstone, wackestone, and packstone. Astronomical the widespread pan-Euramerican cyclothems related to orbital eccentric- calibration of ~3 m sedimentary cycles to a 405 k.y. orbital eccentricity ity forcing (Heckel, 2008); and (3) inconclusive stage-boundary markers cycle period aligns other significant, shorter sedimentary cycles to lead to variable durations for the Carboniferous stages (Ogg et al., 2016). periods recognizable as short orbital eccentricity (136 k.y., 122 k.y., Quantitative biostratigraphic calibration that is separate from the pan- and 96 k.y.), obliquity (31 k.y.), and precession (22.9 k.y. and 19.7 k.y.). Euramerica region needs to be investigated in order to improve Carbonifer- The orbital eccentricity has long-period modulations with 2.4 m.y., 1.6 ous chronology. A near-continuously deposited, carbonate slope succession m.y., and 1.2 m.y. periods, and the obliquity has a 1.2 m.y. modulation at Naqing in South China constitutes an excellent stratigraphic standard for cycle. The astronomical calibration indicates durations of 7.6 m.y., 8.1 the marine Carboniferous in the Paleo-Tethyan realm. Four global strato- m.y., 8.5 m.y., 2.87 m.y., and 4.83 m.y. for the Serpukhovian, Bashkirian, type section and point (GSSP) candidates for the Carboniferous stages have Moscovian, Kasimovian, and Gzhelian Stages, respectively. The cali- been proposed in this section, including Visean/Serpukhovian, Bashkirian/ brated durations of the 25 conodont zones collectively indicate a 33.9 Moscovian, Moscovian/Kasimovian, and Kasimovian/Gzhelian boundaries m.y. time scale. Biochronological correlation of the Paleo-Tethyan and (Ueno and Task Group, 2009; Richards and Task Group, 2010; Qi et al., pan-Euramerican records significantly refines the global chronostratig- 2012, 2016). Here, we present a detailed cyclostratigraphic study using raphy for the Serpukhovian Stage and the Pennsylvanian subsystem. magnetic susceptibility (MS) measurements of the Naqing section and This new Paleo-Tethyan astronomical time scale opens a new window propose a 33.9 m.y. astronomical time scale (ATS) for the Serpukhovian for understanding the late Paleozoic icehouse world. Stage and the stages of the Pennsylvanian subsystem.

INTRODUCTION DATA AND METHODS The Carboniferous Period is a key interval in the evolution of the The South China Block (SCB) was located in an equatorial region Earth system, characterized by major tectonic (Torsvik and Cocks, 2004), adjacent to the eastern Paleo-Tethys Ocean during the Carboniferous climatic (Montañez and Poulsen, 2013), and biotic (Wang et al., 2013) (Fig. 1A). The studied ~250-m-thick Carboniferous section at Naqing events. Reconstruction of the sequence of geological events for the period (25°15′3.9″N, 106°29′6.9″E) in the Guizhou Province includes the Shan- requires an accurate global chronostratigraphic framework. The age model gruya and Nandan Formations, which were deposited in the Qian-Gui for the Carboniferous in the Geologic Time Scale 2012 (GTS2012; Davy- Basin in the southwestern part of the SCB (Figs. 1B and 1C; Fig. DR1 dov et al., 2012) was derived from 405-k.y.-calibrated cyclothems and in the GSA Data Repository1). The lithology is mainly composed of gray, constrained optimization (CONOP) for scaling biozones relative to their thin- to medium-bedded lime mudstone, wackestone, and packstone sediment thicknesses, mostly from pan-Euramerican records. Recently, the intermittently intercalated with chert, which were deposited in a carbonate Pennsylvanian age model for pan-Euramerican successions was revised slope environment without evident hiatuses (Chen et al., 2018; Fig. 1C). using an astronomical calibration of major cyclothems in the Geologic 1 GSA Data Repository item 2019036, additional details of paleoclimatic and *E-mail: [email protected] paleoenvironmental proxies, time series analysis methods, amplitude modulations CITATION: Wu, H., et al., 2018, An ~34 m.y. astronomical time scale for the of the astronomical parameters, Figures DR1–DR7, and Tables DR1–DR3, is uppermost Mississippian through Pennsylvanian of the Carboniferous System of available online at http://www.geosociety.org/datarepository/2019/, or on request the Paleo-Tethyan realm: Geology, v. 47, p. 1–4, https://doi.org/10.1130/G45461.1 from [email protected].

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Figure 1. A: Carboniferous paleogeographic map showing location of 104°E 107°E South China (ca. 300 Ma). Base map is modified from Ron Blakey (http:// A B Guiyang Duyun Panthalassic UralianSiberia Seawa jan.ucc.nau.edu/~rcb7). B: Paleogeographic map of Guizhou Prov- Ocean South China Block Anshun 26°N y Qian-Gui Basin ince and adjacent area, modified from Jiao et al. (2003). C: Lithology, Mid-continent Basin biostratigraphy, and cyclostratigraphy of Naqing section. Conodont Donets Basin Paleo-Te Qujing S. Urals Ocean zones are after Hu (2016). Interpreted 405 k.y. orbital eccentricity cycles thys Naqing (E; red curve) were extracted using a Gaussian filter with pass-bands Gondwana Land Paralic facies 0 40 km of 0.25 ± 0.13 cycles/m for 0–94.8 m, 0.4 ± 0.14 cycles/m for 94.8–159.75 Platform Slope Basin m, 0.3 ± 0.12 cycles/m for 159.75–224.4 m, and 0.4 ± 0.16 cycles/m for 224.4–249.55 m, respectively. M—lime mudstone; W—wackestone; F— C Magnetic fine-grained packstone; C—coarse-grained packstone. Conodont susceptibility (in log) poc h

Depth (m) E Stage zone Lithology -9 -8 -7 E84 Streptognathodus The basal Serpukhovian, Bashkirian, Moscovian, Kasimovian, Gzhelian, Formation wabaunsensis E82 n 240 Streptognathodus E80 and Asselian Stages at Naqing have been defined as the first appearance tenuialveus datum (FAD) of Lochriea ziegleri at 17.92 m, Declinognathodus nodu- Streptognathodus E78 230 virgilicus E76 liferus sensu lato at 91.4 m, Diplognathodus ellesmerensis at 138.15 m, Gzhelia Idiognathodus E74 nashuiensis Idiognathodus turbatus at 200.08 m, I. simulator at 220.33 m, and Strep- 220 Idiognathodus E72 simulator tognathodus isolatus at 249.52 m, respectively (Qi et al., 2012, 2014; Hu Streptognathodus E70 210 zethus E68 Late Pennsylvanian

and Qi, 2017; Hu, 2016; Fig. 1; Fig. DR2 and Table DR1). Kasimo -vian Idiognathodus E66 A high-resolution MS record with 4992 samples, collected at a spac- 200 eudoraensis Idiognathodus E64 ing of 5 cm, is presented for the upper Visean to uppermost Gzhelian guizhouensis E62 190 Idiognathodus Stages (Table DR2). Cyclostratigraphic analysis involves identification of magnificus E60 180 Idiognathodus astronomical frequencies in sedimentary records to construct precise time turbatus E58 scales (Hinnov, 2013). The 2 multitaper method (MTM) spectral analysis Swadelina π 170 makhlinae E56

(Thomson, 1982) was applied with classical red noise modeling reported at Nandan Swadelina E54

Moscovian subexcelsa 160 E52 85%, 90%, 95%, and 99% confidence levels. The evolutionary fast Fourier Idiognathodus podolskensis E50 transform (FFT) spectrogram was computed to identify the changes in 150

Middle Pennsylvanian Mesogondolella E48 donbassica cycle frequencies due to variable sedimentation rates. The MTM and FFT - Mesogondolella E46 analyses use MATLAB scripts available at http://mason.gmu.edu/ ~lhin- 140 clarki E44 Diplognathodus E42 nov/cyclostratigraphytools.html. The interpreted astronomical signals were 130 ellesmerensis E40 “Streptognathodus” E38 extracted with Gaussian band-pass filters in Analyseries 2.0.8 (Paillard et n expansus M2 120 E36 al., 1996). The 405-k.y.-calibrated MS time series was linearly interpolated “Streptog- E34 nathodus” and resampled to a uniform spacing of 5 k.y. (see the Data Repository). expansus M1 E32 110 ashkiria E30 Idiognathodus primulus E28 100 E26

RESULTS Early Pennsylvanian Neognathodus symmetricus MS values range from −4.29 × 10−9 to 4.2 × 10−8 m3/kg, with an average 90 E24 Idiognathoides of 2.59 × 10−9 m3/kg (Fig. 1). The Naqing MS series shows a pattern of cen- sinuatus 80 E22 timeter- to meter-scale lithological rhythms (Fig. DR2). Lime mudstone Declinognathodus noduliferus E20 generally has higher MS values than packstones or wackestones (Fig. 1; 70

nB Gnathodus Fig. DR4). Low and high temperature-dependent magnetic measurements postbilineatus E18 60 ? and hysteresis loops indicate that the magnetic signal is mainly carried by Gnathodus bilineatus E16 paramagnetic clays and diamagnetic carbonate, with minor magnetite and 50 bollandensis E14

high-coercivity particles (e.g., hematite; Fig. DR3). The MS, anhysteretic Serpukhovia E12 40 Late Mississippian remanent magnetization (ARM), and Th series have a comparable relation- Shangruya Lochriea ziegleri E10 ship, with minor mismatches (Fig. DR4), indicating that they may share 30 E8 a similar origin. Therefore, MS was used as a proxy for terrestrial input 20 E6 . to the marine system, in which lower sea level induced higher terrestrial Lochriea nodosa E4 e input and higher MS values, and as a tool for cyclostratigraphic analysis 10 Gnathodus E3 sean bilineatus E2 Vi (Da Silva et al., 2013; Wu et al., 2013; Kodama and Hinnov, 2015). Middl Mississi bilineatus 0 - E1 + The thickness of the interval between the basal Serpukhovian and upper- W C Long eccentricity M F most Gzhelian Stages is ~232 m at Naqing (Fig. 1), with a duration of ~32 filter output m.y. according to GTS2016 (Ogg et al., 2016). An average sedimentation Amplitude modulations filtered from the 136 k.y. and 96 k.y. short rate of ~0.73 cm/k.y. provides an initial constraint for the cyclostratigraphic eccentricity components have periodicities at 2.4 m.y., 1.6 m.y., and 1.2 m.y. interpretation. The FFT spectrogram shows that the sedimentation rate is (Fig. DR7). Amplitude modulations filtered from the 31 k.y. obliquity band relatively stable, with three horizons at 94.8 m, 159.75 m, and 224.4 m of the 405-k.y.-calibrated MS time series have a dominant periodicity of where rates appear to change (Fig. 2B). The uncalibrated Naqing power 1.2 m.y. and smaller periods at 2.3 m.y. and 3.0 m.y. (Fig. DR7). spectrum of four subsets of the MS series shows prominent wavelengths at 2.7–3.5 m, 0.66–1.1 m, 0.21–0.28 m, and 0.11–0.14 m (Fig. 2A; Fig. DR5). DISCUSSION According to the ratio of the astronomical parameters for Carboniferous time (Table DR3), these stratigraphic cycles roughly correspond to 405 Evidence for Secular Resonance between Earth and Mars Orbits k.y., 100 k.y., 30 k.y., and 20 k.y. periods when calibrating the 2.7–3.5 m A notable chaotic motion between Earth and Mars occurs when a cycles to the 405 k.y. long eccentricity cycle. The 405 k.y. calibrated Naq- key resonance between the motions of orbital perihelia (g3 and g4 terms) ing power spectrum has significant spectral peaks at 405 k.y., 136 k.y., and nodes (s3 and s4 terms) of Mars and Earth transition from (s4 – s3)

122 k.y., 103 k.y., 96 k.y., 31.1 k.y., 22.9 k.y., and 19.7 k.y. (Fig. 2C; Fig. – 2(g4 – g3) = 0 to (s4 – s3) – (g4 – g3) = 0 (Laskar, 1990; see the Data DR6). Strong peaks also occur at 2.4 m.y., 1.3 m.y., and 0.7 m.y. (Fig. DR6). Repository). Predicted chaotic resonance transitions have been observed

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Naqing, A E eO P 99% GTS2012 95% South China

3.4 0.78 0.47 90% me (Ma ) 1 0.24 me (Ma ) 1.1 0.34 85% Conodont zone Conodont zone Ti Period Epoc h Stage Stage Period Epoc h 0.67 Long eccentricity filter output Ti 0.22 0.17 50% 0.28 299 0.1 0.2 0.16 0.14 0.11 Streptognathodus Streptognathodus - + 299

Power 0.12 wabaunsensis- wabaunsensis 300 Streptognathodus E82 n 300 0.01 fissus Streptognathodus E80 301 Streptognathodus tenuialveus 301 simplex- Streptognathodus E78 302 Streptognathodus virgilicus Gzhelian bellus E76 Gzhelian 302 Idiognathodus e O P 303 Streptognathodus E74 B 240 virgilicus nashuiensis 303 304 Streptognathodus Idiognathodus E72 220 vitali simulator 304 E O Streptognathodus Streptognathodus E70 e 305 zethus Late Pennsylvania Late Pennsylvanian simulator E68 305 200 Streptognathodus Idiognathodus 306 Kasimo . firmus eudoraensis E66 306

Kasimovian Idiognathodus 180 E 307 Idiognathodus P toretzianus guizhouensis E64 307 O 308 Streptognathodus Idiognathodus E62 160 cancellosus magnificus 308 e E60 P 309 Idiognathodus Idiognathodus 140 E sagittalis turbatus E58 309 O 310 Swadelina Streptognathodus makhlinae 310 e subexcelsus- E56 120 E Swadelina 311 Swadelina subexcelsa E54 makhlinae 311 Depth (m ) Idiognathodus 100 312 Neognathodus podolskensis E52 Moscovian Moscovian roundyi- 312 e Mesogondolella E50 O 313 Streptognathodus 80 cancellosus donbassica 313 - Mesogondolella E48 Middle Pennsylvanian E 314 Middle Pennsylvanian Neognathodus clarki medexultimus- E46 314 60 e Diplognathodus P 315 Streptognathodus concinnus ellesmerensis E44 315 40 “Streptog- E 316 Streptognathodus E42 dissectus nathodus” 316 O expansus M2 20 317 Neognathodus E40 “Streptog- 317 Carboniferous

Carboniferous uralicus e nathodus” E38 318 n Declinognathodus expansus M1 0 1 234 5 6 7 8 910 donetzianus E36 318 Frequency (cycles/m) 319 Idiognathodus Neognathodus primulus E34 319 atokaensis Neognathodus Ee OP 320 ashkiria E32

C symmetricus Bashkirian 320 405 12222 Declinognathodus 103 321 marginodosus Idiognathoides E30 45.8 sinuatus 321

1366 996 Idiognathodus Early Pennsylvanian Early Pennsylvanian E28 1 49.5 31.131.1 322 sinuosus Declinog- nathodus 322 68.9 35.6 Neognathodus E26 0.1 323 noduliferus 26.4 22.9 19.7 askynensis E24 323 Power Gnathodus 324 Idiognathoides 0.01 sinuatus postbilineatus E22 324 325 Declinognathodus Gnathodus E20 n nB noduliferus bilineatus 325 E18 326 Gnathodus bollandensis postbilineatus E16 326 000.01 0.02 0.03 0.04 0.05 .06 327 Gnathodus 327 Frequency (cycles/k.y.) bollandensis E14 328 E12 Lochriea Lochriea ziegleri 328

Figure 2. Power spectrum of log-transformed magnetic susceptibil- Serpukhovia 329 Serpukhovia cruciformis E10 ity (MS) series in stratigraphic and time domains. A: 2π multitaper Late Mississippian Late Mississippian 329 E8 method (MTM) power spectrum of MS stratigraphic series. B: Fast 330 Lochriea ziegleri 330 Fourier transform (FFT) spectrogram with 6 m sliding window and E6 0.05 m step. C: 2 MTM power spectrum of 405-k.y.-calibrated MS 331 Lochriea nodosa π Lochriea nodosa E4 331 time series. Significant spectral peaks are labeled in kiloyears. E, sean 332 sean Gnathodus Lochriea mononodosa E2 332 bilineatus bilineatus Vi Mid. M. Mid. M. e, O, and P represent long orbital eccentricity, short orbital eccen- Vi tricity, obliquity, and precession cycles, respectively. Figure 3. Correlation between astronomically calibrated stage bound- aries and conodont zones at Naqing and radioisotopically calibrated in the Cretaceous (Coniacian; Ma et al., 2017) and Carboniferous (early composite standard in Geologic Time Scale 2012 (GTS2012; Davydov Moscovian; Fang et al., 2018). The Naqing record exhibits 2.4 m.y., 1.6 et al., 2012). Orbital eccentricity signal (blue curve) was extracted from m.y., and 1.2 m.y. modulations in the orbital eccentricity and a 1.2 m.y. log-transformed magnetic susceptibility (MS) time series with filter band-pass of 0.00246 ± 0.0003 cycles/k.y. Basal Gzhelian Stage is modulation in the obliquity during the latest Visean to Gzhelian (Fig. assumed to be a global isochronous level. DR7). Thus, the Naqing record may provide geological evidence for five chaotic resonance transitions in the solar system. basal Kasimovian (FAD of I. turbatus; Qi et al., 2012) is two 405 k.y. cycles younger than the traditional definition (FAD of S. subexcelsus) Carboniferous ATS for the Paleo-Tethyan Realm in the pan-Euramerican record (Schmitz and Davydov, 2012). Thus, the A time-calibrated biostratigraphy at Naqing was constructed using 83.7 duration of the Moscovian Stage should increase to ~9 m.y. from the cycles of the 405 k.y. eccentricity from 0 to 33.9 m.y. (Fig. 3). The dura- ~8.2 m.y. in GTS2012, and correspondingly the Kasimovian Stage should tion of the Serpukhovian Stage is estimated as 7.6 m.y., which is similar to shorten from ~3.3 m.y. to ~2.5 m.y. These results are comparable with the GTS2012/2016 (7.7 ± 0.2 m.y.) and close to the Milankovitch cycle–cali- astronomically calibrated durations of 8.5 m.y. and 2.87 m.y. at Naqing. brated Luokun section, South China (7.68 ± 0.15 m.y.; Fang et al., 2018). If the basal Kasimovian is defined as the FAD of I. heckeli (199.15 m; The Bashkirian and Gzhelian Stage durations are estimated as 8.1 Heckel, 2013), the durations of the Moscovian and Kasimovian Stages m.y. and 4.83 m.y., respectively, which are consistent with 8.0 ± 0.2 m.y. at Naqing would be 8.38 m.y. and 2.99 m.y., respectively, showing some and 4.8 ± 0.1 m.y. in GTS2012 (Table DR1). The new definition for the differences compared to those in GTS2012.

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In the Naqing record, conodont sampling is dense, and the chrono- Fang, Q., Wu, H.C., Wang, X.L., Yang, T.S., Li, H.Y., and Zhang, S.H., 2018, As- clines of evolutionary lineages are recognized in the stable depositional tronomical cycles in the Serpukhovian–Moscovian (Carboniferous) marine sequence, South China, and their implications for geochronology and icehouse environment (Qi et al., 2012). Thus, it is reasonable to assume that the dynamics: Journal of Asian Earth Sciences, v. 156, p. 302–315, https://​doi​.org​ local first occurrence datum (FOD) of the index taxon is a good estimator /10​.1016​/j​.jseaes​.2018​.02​.001. of its FAD. The migration problem should also be minimal in this single Heckel, P.H., 2008, Pennsylvanian cyclothems in Midcontinent North America as section of a carbonate slope environment. The ~0.3–0.4 m.y. earlier FAD far-field effects of waxing and waning of Gondwana ice sheets, in Fielding, C.R., Frank, T.D., and Isbell, J.L., eds., Resolving the Late Paleozoic Ice of I. turbatus (I. heckeli) in the Naqing section indicates that it should Age in Time and Space: Geological Society of America Special Paper 441, have appeared in the “LOST BRANCH” cyclothem, i.e., one cyclothem p. 275–289, https://​doi​.org​/10​.1130​/2008​.2441​(19). lower than the “HERTHA” cyclothem in Euramerica. Its absence in the Heckel, P.H., 2013, Pennsylvanian stratigraphy of the northern Midcontinent shelf “LOST BRANCH” cyclothem is likely related to the major regressive and biostratigraphic correlation of cyclothems: Stratigraphy, v. 10, p. 3–40. Hinnov, L.A., 2013, Cyclostratigraphy and its revolutionizing applications in the event that significantly shrank the Midcontinent Sea (Heckel, 2008). 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(e.g., stage-boundary markers) between pan-Euramerica and the Naqing Montañez, I.P., and Poulsen, C.J., 2013, The late Paleozoic ice age: An evolving ATS affords an opportunity to test correlations among more endemic paradigm: Annual Review of Earth and Planetary Sciences, v. 41, p. 629–656, biotas (Fig. 3), which is particularly significant for middle Bashkirian– https://​doi​.org​/10​.1146​/annurev​.earth​.031208​.100118. Ogg, J., Ogg, G., and Gradstein, F., 2016, A Concise Geologic Time Scale 2016: Kasimovian conodonts with high provincialism, and for improvement of Amsterdam, Netherlands, Elsevier, 234 p., https://doi​ ​.org​/10​.1016/B978​ ​-0​ the Carboniferous time scale. -444​-59467​-9​.00001​-7. Paillard, D., Labeyrie, L., and Yiou, P., 1996, Macintosh Program performs time-series CONCLUSION analysis: Eos (Washington, D.C.), v. 77, p. 379, https://​doi.org​ /10​ .1029​ /96EO00259.​ Qi, Y.P., Hu, K.Y., James, E.B., Wang, Q.L., and Lin, W., 2012, Discovery of the Time-series analysis of a continuous carbonate slope succession at conodont lineage from Idiognathodus swadei to I. turbatus in South China Naqing, South China, indicates that rhythmic sedimentation from the and its implications: Journal of Stratigraphy, v. 36, p. 551–557, https://​doi​ upper Visean to uppermost Gzhelian Stages was controlled by astronomi- .org​/10​.3969​/j​.issn​.0253​-4959​.2012​.03​.007. cal forcing, with evidence for chaotic motions between Earth and Mars. Qi, Y.P., Nemyrovska, T.I., Wang, X.D., Chen, J.T., Wang, Z.H., Lane, H.R., Richards, B.C., Hu, K.Y., and Wang, Q.L., 2014, Late Visean–early Serpukhovian conodont The estimated ages and durations of the global stages at Naqing affirm and succession at the Naqing (Nashui) section in Guizhou, South China: Geological extend the published long orbital eccentricity scaling for the Pennsylva- Magazine, v. 151, p. 254–268, https://​doi​.org​/10​.1017​/S001675681300071X. nian “cyclothems” and their U-Pb–dated equivalents in pan-Euramerica. Qi, Y.P., Lambert, L.L., Nemyrovska, T.I., Wang, X.D., Hu, K.Y., and Wang, Q.L., The new data also extend the long orbital eccentricity-calibrated ATS 2016, Late Bashkirian and early Moscovian conodonts from the Naqing sec- tion, Luodian, Guizhou, South China: Palaeoworld, v. 25, p. 170–187, https://​ into the late Mississippian. Future work will extend cyclostratigraphic doi​.org​/10​.1016​/j​.palwor​.2015​.02​.005. analysis into the early Mississippian to complete the Carboniferous ATS. Richards, B.C., and Task Group, 2010, SCCS Annual Report 2009: Newsletter on Carboniferous Stratigraphy, v. 28, p. 14–26. ACKNOWLEDGMENTS Schmitz, M.D., and Davydov, V.I., 2012, Quantitative radiometric and biostrati- We express our sincere appreciation to Geology Editor James Schmitt, and graphic calibration of the Pennsylvanian–Early Permian (Cisuralian) time James Ogg, Kenneth Kodama, Anne-Christine da Silva, and Mark Schmitz for scale and pan-Euramerican chronostratigraphic correlation: Geological Society their careful reviews and constructive suggestions. This work is supported by the of America Bulletin, v. 124, p. 549–577, https://​doi​.org​/10​.1130​/B30385​.1. National Natural Science Foundation of China (41790451, 41688103, 41602025, Thomson, D.J., 1982, Spectrum estimation and harmonic analysis: Proceedings 41630101, and 41422202), the Chinese Academy of Sciences (grants XDB18030400, of the IEEE, v. 70, p. 1055–1096, https://​doi​.org​/10​.1109​/PROC​.1982​.12433. XDB26000000, QYZDY-SSW-DQC023), and the U.S. National Science Foundation Torsvik, T.H., and Cocks, L.R.M., 2004, Earth geography from 400 to 250 Ma: (grants 1337454 and 1543518). This is a contribution to International Geoscience A palaeomagnetic, faunal and facies review: Journal of the Geological Soci- Programme (IGCP) 652 “Reading Geologic Time in Paleozoic Sedimentary Rocks.” ety [London], v. 161, p. 555–572, https://​doi​.org​/10​.1144​/0016​-764903​-098. Ueno, K., and Task Group, 2009, Report of the Task Group to establish the Mosco- vian-Kasimovian and Kasimovian-Gzhelian boundaries: Newsletter on Car- REFERENCES CITED boniferous Stratigraphy, v. 27, p. 14–18. 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