The　timing　and　structure　of　Termination　II　(T-II)　is　still　debatable　as　the　number　of　high-quality　records　is　insufficient.　This　study　presents　precisely　dated　stalagmite　delta　O-18　data　between　133.4　+/-　0.3　to　126.6　+/-　0.3　ka　BP　(covering　most　of　T-11)　from　north　China,　near　the　northern　limit　of　the　East　Asian　summer　monsoon　(EASM),　an　area　sensitive　to　climate　change.　The　onset　of　the　last　interglacial　is　constrained　at　129.4　+/-　0.3　ka　BP,　consistent　with　south　Chinese　speleothem　records,　further　supporting　the　idea　that　Northern　Hemisphere　summer　insolation　plays　an　important　role　in　initiating　glacial　terminations.　An　extended　interval　of　heavy　delta　O-18　is　observed　immediately　prior　to　this　abrupt　transition,　named　as　the　＂Weak　Monsoon　Interval＂　(WMI)　in　south　Chinese　cave　records,　which　was　associated　with　the　Heinrich　Stadial　11　(H11)　in　the　North　Atlantic.　A　significant　millennial-scale　interstadial　peaking　at　132.7　+/-　0.3　ka　BP　is　identified　preceding　the　weakest　phase　of　the　WMI.　A　synchronous　counterpart　is　also　found　in　some　south　Chinese　speleothem　and　North　Atlantic　alkenone　Mg/Ca　SST　records.　It　is　inferred　that　the　main　H11　freshwater　penetration　possibly　occurred　after　131.5　ka　BP,　leaving　some　aspects　of　ocean　and　atmospheric　circulation　still　in　interstadial　mode　from　134　to　131.5　ka　BP.　Following　the　onset　of　the　last　interglacial,　there　was　a　millennial-scale　＂pause＂　in　our　delta　O-18　record,　synchronized　with　a　＂slowdown＂　in　the　rate　of　decrease　in　delta　O-18　in　south　Chinese　cave　records.　This　is　possibly　a　large　regional　climate　oscillation,　as　it　is　also　identified　in　some　North　Atlantic　records,　but　one　which　is　too　weak　to　be　a　Younger　Dryas　(YD)-type　event.　In　summary,　compared　to　south　Chinese　cave　records,　significant　millennial-scale　climate　oscillations　before　and　after　the　synchronous　onset　of　the　last　interglacial　is　the　main　feature　of　our　record.　Nevertheless,　the　sequence　of　these　climate　events　remains　very　different　from　Termination　I　(T-I),　which　is　possibly　ascribed　to　the　stronger　insolation,　higher　atmosphere　CO2,　and　the　resultant　faster　and　greater　meltwater　pulse　to　the　North　Atlantic　during　T-II　than　during　T-I.　(C)　2019　Elsevier　B.V.　All　rights　reserved.