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1 ddle Ordovician-Carboniferous; Late Jurassic-Paleogene).
2 ecialisation among marine snakes through the Paleogene.
3 community in the latest Cretaceous and early Paleogene.
4 meters east of South America during the late Paleogene.
5 ns of the Eurasian landmass during the Early Paleogene.
6 fast sensitivity reach far beyond the early Paleogene.
7 experienced from the Late Cretaceous to the Paleogene (100.5-23.03 mya) in response to major climati
8 younger fossil record (latest Cretaceous and Paleogene, ~75 to 50 Ma) while providing a reliable cali
9 f the angiosperms (flowering plants), then a Paleogene advance to ecological dominance in concert wit
11 liferation of coral reef habitats during the Paleogene also likely facilitated carcharhiniform disper
12 cently, during the Late Cretaceous and early Paleogene, although the exact timing and cause of their
13 et diversification rates occurred during the Paleogene and Miocene (between 30 and 7 Ma) in associati
15 rations relevant for simulation of the early Paleogene, and (iii) fast or "Charney" climate sensitivi
17 f these groups are known to survive into the Paleogene, and their persistence into the latest Maastri
18 ost complete and best-preserved cranium of a Paleogene anthropoid ever found, that of a small female
19 deal of emphasis on the dental evidence for Paleogene anthropoid interrelationships, but cladistic a
20 propliopithecines than they are to any other Paleogene anthropoid taxon, and that Proteopithecus exhi
21 lution of a low-salinity ancestor for a post-Paleogene arc Yucatan + Cuba Typhlatya clade within the
24 vely different changes before the Cretaceous-Paleogene asteroid impact, which should be considered wh
26 arming event (LMWE), preceded the Cretaceous-Paleogene boundary (KPB) mass extinction at 66.05 0.08 M
28 the crater formed at or near the Cretaceous-Paleogene boundary (~66 million years ago), approximatel
29 t establish synchrony between the Cretaceous-Paleogene boundary and associated mass extinctions with
30 diversity declined by 45% at the Cretaceous-Paleogene boundary and did not recover for ~6 million ye
31 itiated ~250,000 years before the Cretaceous-Paleogene boundary and that >1.1 million cubic kilometer
34 drop in delta(7)Li(SW) across the Cretaceous-Paleogene boundary cannot be produced by an impactor or
36 topes in samples taken from three Cretaceous-Paleogene boundary sites, five other impacts that occurr
38 hness abruptly tripled across the Cretaceous/Paleogene boundary, but did not increase over the next 6
39 of East Asia and Europe near the Cretaceous-Paleogene boundary, probably via a continuous paleo-rive
40 nt estimated to be present at the Cretaceous-Paleogene boundary, produce what might have been one of
41 igate goethite spherules from the Cretaceous-Paleogene boundary, revealing the internal elemental dis
42 ion of non-avian dinosaurs at the Cretaceous-Paleogene boundary, triggered ecological diversification
43 extinction of pachycormids at the Cretaceous-Paleogene boundary, which is consistent with an opportun
44 can eruptive activity spanned the Cretaceous-Paleogene boundary, which is renowned for the extinction
53 vely cool temperatures across the Cretaceous-Paleogene boundary; there is no indication of a major wa
55 ortunity' during the Ordovician and Jurassic-Paleogene capable of supporting dramatic expansions of p
58 ird clade of anthropoids was involved in the Paleogene colonization of South America by primates.
60 odies followed during the Cretaceous and the Paleogene, convergently giving rise to the classic toads
62 sisted throughout much of the Mesozoic-early Paleogene due to an expanded tropical belt and more equa
63 ith more generalized taxa from the Laurasian Paleogene (e.g., geolabidids, nyctitheriids, leptictids)
64 Previous paleobotanical work concluded that Paleogene elements of the sclerophyllous subhumid vegeta
69 occurred in the Neoaves after the Cretaceous-Paleogene extinction rather than earlier in bird evoluti
70 nd biotic collapses that mark the Cretaceous-Paleogene extinction, are poorly resolved despite extens
74 -Lopingian, Permian-Triassic, and Cretaceous-Paleogene extinctions where the proportion of large gene
75 ional anatomy in mineralized arthropods from Paleogene fissure fillings and demonstrate the value of
77 e area through time, we illustrate that most Paleogene fossil-bearing localities would have been suit
78 dition, a rich new harvest of Cretaceous and Paleogene fossils has helped to date the major evolution
79 agnitude of warming reconstructed from early Paleogene greenhouse climates and demands a close examin
80 arine coarse siliciclastic response to early Paleogene hothouse climatic and oceanographic conditions
81 m LPEE warming (~58 Ma), and the two largest Paleogene hyperthermals, the Paleocene-Eocene Thermal Ma
82 diversity on land during the Mesozoic-early Paleogene interval, applying sample-standardization to a
84 at the backbone occurred near the Cretaceous-Paleogene (K-Pg) boundary (65 Mya) which is consistent w
85 ntensively studied event is the Cretaceous - Paleogene (K-Pg) boundary (ca. 66 million years ago [MYA
86 illion years ago, Ma) between the Cretaceous-Paleogene (K-Pg) boundary and the Paleocene-Eocene Therm
89 covery of life in response to the Cretaceous-Paleogene (K-Pg) boundary mass extinction ~ 66 million y
90 s and peak diversification at the Cretaceous-Paleogene (K-Pg) boundary support the longstanding hypot
92 in core Lamiales (CL) around the Cretaceous-Paleogene (K-Pg) boundary, and seven more in EDL relativ
93 before and immediately after the Cretaceous-Paleogene (K-Pg) boundary, implying important roles for
94 gin of placentals relative to the Cretaceous-Paleogene (K-Pg) boundary, we scored 4541 phenomic chara
98 lide impact, is implicated in the Cretaceous-Paleogene (K-Pg) extinction approximately 66 million yea
101 their final disappearance at the Cretaceous-Paleogene (K-Pg) mass extinction event 66 Mya has been d
104 equence of events that led to the Cretaceous-Paleogene (K-Pg) mass extinction of 76% species, includi
105 tal mammals originated before the Cretaceous-Paleogene (K-Pg) mass extinction, anywhere from the Late
108 sociated with the end-Cretaceous [Cretaceous-Paleogene (K-Pg)] mass extinction limit our understandin
109 ion of species richness after the Cretaceous/Paleogene (K/Pg) boundary deserves further examination i
110 he extinction of dinosaurs at the Cretaceous/Paleogene (K/Pg) boundary was the seminal event that ope
112 terrestrial tetrapods through the Cretaceous-Paleogene (K/Pg) mass extinction (Campanian-Ypresian).
113 nsequences of the end-Cretaceous [Cretaceous/Paleogene (K/Pg)] mass extinction persist in present-day
115 aceous Terrestrial Revolution and Cretaceous-Paleogene (KPg) mass extinction in opening up ecospace t
117 gly skewed towards the tropics from the late Paleogene, likely steepening the latitudinal biodiversit
118 s of ammonite survival across the Cretaceous-Paleogene (Maastrichtian-Danian) boundary, based on new
120 has produced Afro-Arabia's primary record of Paleogene mammalian evolution, including the world's mos
123 115 million years ago; before the Cretaceous-Paleogene mass extinction and ~30 million years prior to
125 logical upheavals produced by the Cretaceous-Paleogene mass extinction event (K-Pg, -66 Ma) have been
126 n bird orders diverged before the Cretaceous-Paleogene mass extinction event 66 million years ago ins
127 ostly stable until the end of the Cretaceous-Paleogene mass extinction event 66 million years ago.
128 uring a rapid radiation after the Cretaceous-Paleogene mass extinction event about 66 million years a
130 lone among dinosaurs survived the Cretaceous-Paleogene mass extinction is crucial to reconstructing t
131 suggests a possible impact of the Cretaceous-Paleogene mass extinction on their radiation and that Br
132 d rapidly in the aftermath of the Cretaceous-Paleogene mass extinction within Neoaves, in which multi
135 the stage as main drivers of the Cretaceous-Paleogene mass extinction-Deccan Traps volcanism, and an
139 -Triassic, Triassic-Jurassic, and Cretaceous-Paleogene mass extinctions were geologically rapid, wher
140 the two taxa likely diverged during the late Paleogene near or after the onset of volcanism that prod
141 n North America and subsequently crossed the Paleogene North Atlantic land bridge (NALB) to Europe.
143 he genus by at least 10 million years in the Paleogene of Asia, which closes the gap between Mimolagu
144 d mammalian lineage of African origin in the Paleogene of South America-a newly discovered genus and
145 0 to 40 Ma from Australia (Late Triassic and Paleogene of Tasmania; Late Cretaceous Gippsland Basin i
146 tion of tarsiers relative to anthropoids and Paleogene omomyids remains a subject of lively debate th
149 and postcranium of certain poorly understood Paleogene primates are clearly needed to help test wheth
150 estimates of the Late Eocene and Cretaceous/Paleogene projectiles are within 50% of independent esti
152 wide structure buried below ~300 to 400 m of Paleogene sediment with characteristics consistent with
156 f the chronological evidence shared by later Paleogene strata exposed in Egypt and Oman (Taqah and Th
157 molluscs) from a highly expanded Cretaceous-Paleogene succession: the Lopez de Bertodano Formation o
158 important role in maintaining elevated early Paleogene temperatures, (ii) radiative forcing by carbon
160 locality in eastern Peru produced the first Paleogene vertebrate fauna from the Amazon Basin, includ
163 ditions during the late Cretaceous and early Paleogene were coupled with diversification events of ma
164 thin a single biogeographic realm during the Paleogene, with a few long-distance dispersal events.
165 endemism in the latest Cretaceous and early Paleogene, with bioprovinces shaped by temperature and g