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All graphs considered in this paper are finite, undirected and simple. Let G be a graph with vertex-set V(G) and edge-set E(G). A subset D of V(G) is called a dominating set of G if every vertex of G is either in D or adjacent to a vertex of D. The domination number γ(G) is the cardinality of a minimum dominating set of G.
The domination in graphs is so classic that it has been widely studied in networks theory, while the decision problem for the domination number of a general graph was proved to be NP-complete [8]. On the study of domination, there are three early textbooks compiled by Haynes et al. [13,14] and Henning et al. [17]. Recently, Haynes, Hedetniemi and Henning [11,12] edited two new books on this field once again.
Definition 1.1. [24] (1) A vertex v∈V(G) is called γ-fixed if v belongs to every minimum dominating set of G. (2) A vertex v∈V(G) is called γ-bad if v does not belong to any minimum dominating set of G. (For simplicity, we abbreviate "γ-fixed" and "γ-bad" to "fixed" and "bad" respectively in this paper.)
Definition 1.2. A vertex v∈V(G) is called critical if γ(G−v)<γ(G). In particular, we agree that the single vertex of a trivial graph is critical.
Remark for Definition 1.2: It is easy to see that γ(G−v)<γ(G)⇔γ(G−v)≤γ(G)−1⇔γ(G−v)=γ(G)−1, where γ(G−v)≤γ(G)−1⇒γ(G−v)=γ(G)−1 holds because if not so, then γ(G−v)≤γ(G)−2, and thus G would have a dominating set with cardinality ((γ(G)−2)+|v|)<γ(G), contradicting the minimality of γ(G).
The terms of fixed and bad vertices of graphs were introduced by Samodivkin [24], which can help us to research the constructions of minimum dominating sets of a graph better and shorten the processes of our proofs [7,22,24,25]. (In [28], fixed and bad vertices of a graph are also called universal and idle vertices, respectively.) The notions of domination critical, which include vertex-critical [4] and edge-critical [3,27], are very important to domination of graphs. But in this paper, we are not going to discuss the topic of edge-critical.
Definition 1.3. A graph G is called vertex-critical if every vertex of G is critical.
There are lots of nice properties on domination vertex-critical graphs [1,2,19,29,30]. Many of them possess symmetry, and even vertex-transitivity. For example, the graph C4⋅C4 obtained by identifying two vertices of two cycles of orders four, the Harary graph H3,8 and the circulant graph C12⟨1,5⟩ (See Figure 1.).
Trees is a kind of basic graph class often applied to algorithm design. There are a good few results on the study of the constructions for special trees, such as trees with equal domination and total domination numbers [7], trees with equal domination and restrained domination numbers [6], trees with equal total domination and disjunctive domination numbers [18], trees with equal independent domination and weak domination numbers [10], trees with a minimum vertex cover also being a minimum total dominating set [5], trees with two disjoint minimum independent dominating sets [15], trees with the paired domination number being twice the matching number [26], trees without fixed vertices [31], trees without fixed vertices and critical vertices [23,16], trees with unique minimum dominating sets [9,34], trees with equal Roman {2}-domination and Roman domination numbers [21], and trees with total Roman domination number being equal to the sum of domination number and semitotal domination number [20].
Naturally, there are two such questions: Can we exhaustively characterize vertex-critical graphs, as well as graphs without critical vertices? It seems not easy to solve these two questions. Therefore, in this paper, we study on the latter one and focus on the graph class-trees. Via defining 3 operations of graphs, we get a constructive characterization of trees without critical vertices.
For any u,v∈V(G), denote by dG(u,v) the distance from u to v in G as well as dG(v), NG(v), NG[v] and N2G(v) the degree, open neighborhood, closed neighborhood and 2-open neighborhood of vertex v in G respectively, where the 2-open neighborhood of vertex v in G is defined as N2G(v)={x∈V(G)∣d(x,v)=2}. For any ∅≠X⊆V(G), let G[X] denote the subgraph of G induced by X.
Denote by MDS_(G) the set composed of all the minimum dominating sets of G. That is, MDS_(G)={D∣D is a minimum dominating set of G}. A vertex of degree one (resp. degree zero) in G is called an end-vertex (resp. isolated vertex) of G. Let g be a cut-vertex of G. If a component P of G−g is a path and g is adjacent to an end-vertex of P in G, then we call P as a pendant path of G and say that g and P are linked with each other. A pendant path of G with order l (l≥1) is called an l-pendant path of G. Let P2k+1=v1v2⋯v2k+1 be a path of order 2k+1. Then vk+1 is the center of P2k+1.
Let r be a vertex, l and m be two non-negative integers with l+m≥1. Let P13≅P23≅⋯≅Pl3≅P3 with Pi3=viuiwi, i=1,2,…,l, and P12≅P22≅⋯≅Pm2≅P2 with Pj2=xjyj, j=1,2,…,m. For every 1≤i≤l, link r and ui by an edge. For every 1≤j≤m, link r and xj by an edge. Denote the resulting graph as Rl,m and call r as the root of Rl,m (See Figure 2).
Now, we give three observations and some known lemmas, which will support our proofs in the next section.
Observation 2.1. Let G be a graph. If G1 and G2 are vertex-induced subgraphs of G such that V(G)=V(G1)∪V(G2), then γ(G)≤γ(G1)+γ(G2) with the equality holding when G1 and G2 are two components of G.
Observation 2.2. Let u∈V(G). If u is adjacent to two end-vertices v and w in G, then v and w are bad in G, and u is fixed in G.
Observation 2.3. Let u be an end-vertex of G with NG(u)={v}. Then u is non-fixed and v is non-bad in G, and |{u,v}∩D|=1 for any D∈MDS_(G).
Lemma 2.4. [3] For any nontrivial tree T and any v∈V(T), v is a fixed vertex of T if and only if γ(T−v)>γ(T).
Lemma 2.5. [32] Let G be a graph with minimum degree at least one. If x is a bad or fixed vertex of G, then all the elements of NG[x] are non-critical vertices of G.
Lemma 2.6. [33] Let G be a graph.
(a) If x is a non-fixed vertex of G, then γ(G−x)≤γ(G).
(b) If x is a bad vertex of G, then γ(G−x)=γ(G).
(c) If x is a non-fixed and non-critical vertex of G, then γ(G−x)=γ(G).
Lemma 2.7. [34] Let T be a tree containing only one vertex u of degree at least 3. Then u is linked with |NT(u)| pendant paths in T.
Lemma 2.8. [34] Let T be a tree with at least two vertices of degree at least 3 and let dT(u,v)=max{dT(x,y)| both x and y are vertices of degree at least 3 in T}. Then u is linked with |NT(u)|−1 pendant paths in T.
Lemma 2.9. [34] Let G0 be a graph without any isolated vertices and possessing a fixed vertex. If G is a graph obtained via linking a fixed vertex of G0 and the single vertex of P1 by an edge, then γ(G)=γ(G0).
Lemma 2.10. [34] Let G0 be a graph without any isolated vertices and possessing a fixed vertex. If G is a graph obtained via linking a fixed vertex of G0 and the center of P3 by an edge, then γ(G)=γ(G0)+1.
We now ask a question: Is there a nontrivial tree only containing critical vertices? Unluckily, the answer to this question is no (See Lemma 3.1).
Lemma 3.1. If dG(u)=1 and v∈NG(u)∪N2G(u), then v is a non-critical vertex of G.
Proof. Suppose to the contrary that v is a critical vertex of G. If v∈NG(u), let D1∈MDS_(G−v). Then by Definition 1.2, we have |D1|=γ(G)−1. Since u is an isolated vertex of G−v, it follows that u is fixed in G−v. Now, if we let D2=(D1−{u})∪{v}, then D2 is a dominating set of G with |D2|=|D1|=γ(G)−1, a contradiction.
If v∈N2G(u), then |D′|=γ(G)−1 for any D′∈MDS_(G−v). Let NG(u)={w}. Since u is still an end-vertex of G−v, it follows from Observation 2.3 that w is a non-bad vertex of G−v. Let D′1∈MDS_(G−v) with w∈D′1. On one hand, we have |D′1|=γ(G)−1. But on the other hand, D′1 is also a dominating set of G, which implies that |D′1|≥γ(G), a contradiction.
Lemma 3.1 tells us that if G is nontrivial and has an end-vertex, then G must have a non-critical vertex. Therefore, a tree is vertex-critical if and only if it is trivial.
In this subsection, via several operations of graphs, we can get large graphs without critical vertices from small graphs without critical vertices step by step. In particular, these processes of operations are reversible for trees. (Here, large graph represents graph with large order while small graph represents graph with small order.) For a graph G0, we define the following three operations.
Operation i. Link a fixed vertex of G0 and the single vertex of P1 by an edge. Denote the resulting graph by G0∽P1. (Refer to Figure 3 (i)).
Operation ii. Link a fixed vertex of G0 and the center of P3 by and edge. Denote the resulting graph by G0∽P3. (Refer to Figure 3 (ii)).
Operation iii. Link an arbitrary vertex of G0 and the root of Rl,m by and edge. Denote the resulting graph by G0∽Rl,m. (Refer to Figure 3 (iii)).
Remark. In fact, the resulting graph may be not unique. So, "G=G0∽P1" means that "G is obtained from G0 by Operation i".
Lemma 3.2. Let G0 be a graph without any isolated vertices and possessing a fixed vertex, and let G=G0∽P1. Then all the vertices of G0 are non-critical if and only if all the vertices of G are non-critical.
Proof. (⇒) Suppose that V(P1)={v1} and gv1∈E(G). From Lemma 2.9, we have γ(G)=γ(G0)=γ(G−v1). So by Definition 1.2, v1 is a non-critical vertex of G. Also, we have g is a non-critical vertex of G by Lemma 3.1. It remains to prove that x is a non-critical vertex of G for every x∈V(G−v1−g)⊆V(G0). Since all the vertices of G0 are non-critical, we have γ(G0−x)≥γ(G0). Since dG−x(v1)=1, we have v1 is a non-fixed vertex of G−x by Observation 2.3. So there exists D−x∈MDS_(G−x) such that v1∉D−x, and then g∈D−x. Thus D−x∩V(G0−x) is a dominating set of G0−x. Hence γ(G−x)=|D−x|=|D−x∩V(G0−x)|≥γ(G0−x)≥γ(G0)=γ(G), which implies that x is a non-critical vertex of G. The necessity follows.
(⇐) Assume to the contrary that G0 has a critical vertex y0. Since all the vertices of G are non-critical, we have γ(G−y0)≥γ(G). Let D−0∈MDS_(G0−y0). Then |D−0∪{y0}|=γ(G0−y0)+1=γ(G0), which implies that D−0∪{y0}∈MDS_(G0). By the definition of Operation i, g is a fixed vertex of G0. So we have g∈D−0∪{y0}, and g is a non-critical vertex of G0 by Lemma 2.5. Thus g≠y0, and therefore g∈D−0, which implies that D−0 is a dominating set of G−y0. Hence γ(G0−y0)=|D−0|≥γ(G−y0)≥γ(G)=γ(G0), which contradicts the assumption that y0 is a critical vertex of G0. The sufficiency follows.
Lemma 3.3. Let G0 and W be two graphs. Let G be a graph obtained via linking an arbitrary vertex of G0 and an arbitrary vertex of W by an edge. If γ(G)=γ(G0)+γ(W) and all the vertices of G are non-critical, then all the vertices of G0 are non-critical.
Proof. For any y∈V(G0), since all the vertices of G are non-critical, it follows that γ(G−y)≥γ(G). By Observation 2.1, we have γ(G0−y)+γ(W)≥γ(G−y)≥γ(G)=γ(G0)+γ(W). Thus γ(G0−y)≥γ(G0), and so y is a non-critical vertex of G0. The lemma follows.
Lemma 3.4. Let G0 be a graph without isolated vertices and possessing a fixed vertex, and G=G0∽P3.
(a) If all the vertices of G are non-critical, then all the vertices of G0 are non-critical.
(b) When G0 is a tree, (in order to avoid confusion, ) we rewrite T0=G0 and T=G. If all the vertices of T0 are non-critical, then all the vertices of T are non-critical.
Proof. (a) Suppose that P3=v1v2v3 and E(G)−E(G0)−E(P3)={gv2}. Then g is fixed in G0. From Lemma 2.10, we get γ(G)=γ(G0)+1. Item (a) follows by Lemma 3.3.
(b) Firstly, by Observation 2.2, v2 is a fixed vertex of T. So by Lemma 2.5, v1,v2, v3 and g are non-critical vertices of T.
Secondly, we need to show that x is a non-critical vertex of T for every x∈V(T−g)−V(P3). That is, to prove γ(T−x)≥γ(T). Since T0 has no critical vertices, we have γ(T0−x)≥γ(T0). Let D−x∈MDS_(T−x). If g∈D−x, then D−x∩V(T0−x) is a dominating set of T0−x, and so γ(T−x)=|D−x|=|D−x∩V(T0−x)|+|{v2}|≥γ(T0−x)+1≥γ(T0)+1=γ(T). If g∉D−x, then (D−x∩V(T0−x))∪{x} is a dominating set of T0−g. By Lemma 2.4, we have |(D−x∩V(T0−x))∪{x}|≥γ(T0−g)≥γ(T0)+1, which implies that |D−x∩V(T0−x)|≥γ(T0). So γ(T−x)=|D−x|=|D−x∩V(T0−x)|+|{v2}|≥γ(T0)+1=γ(T). Item (b) follows.
Note. In Lemma 3.4 (b), we restrict G0 to be a tree because if G0 is a general graph, then the result maybe not true. (See the following Example 3.5).
Example 3.5. Define G0 and G as shown in Figure 4. Then G=G0∽P3. It is not hard to check that γ(G0)=2, h1 and g are fixed vertices of G0, as well as w1,u1,u2,u3,u4 and h2 are bad vertices of G0. By Lemma 2.5, G0 has no critical vertices. However, since γ(G)=γ(G0)+1=3, we can see that {h2,v2}∈MDS_(G−w1), which implies that w1 is a critical vertex of G.
Lemma 3.6. Let G0 be a graph and G=G0∽Rl,m. Then
(a)γ(G)=γ(G0)+(l+m);
(b) all the vertices of G0 are non-critical if and only if all the vertices of G are non-critical.
Proof. Suppose that E(G)−E(G0)−E(Rl,m)={gr}. Set U={u1,u2,…,ul}, X={x1,x2,…,xm}, Y={y1,y2,…,ym} and Z=X∪Y.
(a) We can easily see that γ(Rl,m)=l+m. So γ(G)≤γ(G0)+(l+m). It remains to prove γ(G)≥γ(G0)+(l+m). Let D∈MDS_(G). If D∩V(G0) can dominate g in G, then D∩V(G0) is a dominating set of G0, and so |D|≥|D∩V(G0)|+|U|+|D∩Z|≥γ(G0)+(l+m); if not, then r∈D and (D∩V(G0))∪{g} is a dominating set of G0, and so |D|=|D∩V(G0)|+|{r}|+|U|+|D∩Z|=|(D∩V(G0))∪{g}|+(l+m)≥γ(G0)+(l+m).
(b) (⇐) The sufficiency follows immediately by Item (a) and Lemma 3.3.
(⇒) We claim that r is a bad vertex of G. Otherwise, let Dr∈MDS_(G) with r∈Dr. If g∈Dr, then Dr−{r} is a dominating set of G, contradicting the minimality of |Dr|. So we have g∉Dr, and then Dr∩V(G0) is a dominating set of G0−g. Thus γ(G0−g)≤|Dr∩V(G0)|=|Dr|−|U|−|Dr∩Z|−|{r}|=γ(G)−(l+m)−1=γ(G0)−1, which implies that g is a critical vertex of G0, contradicting the known condition that G0 has no critical vertices.
Now firstly, for every 1≤i≤l and every 1≤j≤m, we have ui,vi,wi,r,g and xj are non-critical vertices of G by Lemma 2.5.
Secondly, if there exists some 1≤j′≤m such that γ(G−yj′)=γ(G)−1, we can let D−∈MDS_(G−yj′) with r∈D− by Observation 2.3. But then D−∪{yj′}∈MDS_(G) with r∈D−∪{yj′}, contradicting the claim that r is bad in G. So for every 1≤j≤m, we have γ(G−yj)≥γ(G), which implies that yj is non-critical in G.
Finally, it remains to show that γ(G−x)≥γ(G) for every x∈V(G−g)−V(Rl,m)⊆V(G0). Since all the vertices of G0 are non-critical, we have γ(G0−x)≥γ(G0). Let D−x∈MDS_(G−x). If D−x∩V(G0−x) can dominate g, then D−x∩V(G0−x) is a dominating set of G0−x, and so γ(G−x)=|D−x|≥|D−x∩V(G0−x)|+|U|+|D−x∩Z|≥γ(G0−x)+(l+m)≥γ(G0)+(l+m)=γ(G); if not, then we have r∈D−x and (D−x∩V(G0−x))∪{g} is a dominating set of G0−x, and so γ(G−x)=|D−x|=|D−x∩V(G0−x)|+|{r}|+|U|+|D−x∩Z|=|(D−x∩V(G0−x))∪{g}|+(l+m)≥γ(G0−x)+(l+m)≥γ(G0)+(l+m)=γ(G). The necessity follows.
Since it is hard to obtain a constructive characterization of graphs without critical vertices, we only solve this problem partly by restricting the graph class to be trees in this subsection.
Theorem 3.7. A nontrivial tree T has no critical vertices if and only if T can be obtained from P2 or P3 by a finite sequence of Operations i–iii.
Proof. Let T be the set of graphs obtained from P2 or P3 by a finite sequence of Operations i–iii. It suffices to prove that T has no critical vertices if and only if T∈T.
(⇐) Assume that T is obtained by doing n times Operations i, ii and iii. We will prove that all the vertices of T are non-critical by induction on n. When n=0, we have T=P2 or T=P3, and the result is true clearly. Suppose that the result is true when n=k(k≥0). Then from Lemmas 3.2, 3.4 (b), and 3.6 (b), we know that the result is also true when n=k+1. By the induction principle, the sufficiency follows.
(⇒) We are going to prove the necessity by induction on |V(T)|. When |V(T)|=2 or 3, the result is true clearly. Suppose that the result is true when |V(T)|<k(k≥4). We consider the case when |V(T)|=k below.
Case 1. T has a pendant path of order at least 3.
Let P3 be a 3-pendant path of T and T0=T−V(P3). Note that P3≅R0,1. So T=T0∽R0,1. By Lemma 3.6 (b), all the vertices of T0 are non-critical. Since |V(T0)|<|V(T)|=k, we have T0∈T by the induction hypothesis. Hence T=T0∽R0,1∈T.
Case 2. T has a vertex u adjacent to an end-vertex w in T and u is fixed in T−w.
Let T0=T−w. Then T=T0∽P1. By Lemma 3.2, T0 has no critical vertices. Since |V(T0)|=k−1<k, we have T0∈T. Hence T=T0∽P1∈T.
Case 3. T has a vertex u of degree 3 which is adjacent to two end-vertices v,w of T and a fixed vertex g of T−{v,u,w} in T.
Let T0=T−{v,u,w}. Then T=T0∽P3. By Lemma 3.4 (a), T0 has no critical vertices. So T0∈T, and hence T∈T.
Case 4. T has a vertex u of degree at least 3 linked with |NT(u)|−1 2-pendant paths.
Let P12,P22,…,Pm2 be the 2-pendant paths linked with u in T, where m=|NT(u)|−1. Then T[{u}∪⋃mj=1V(Pj2)]≅R0,m. Let T0=T−({u}∪⋃mj=1V(Pj2)). Then T=T0∽R0,m. As a consenquence, we have T∈T.
Case 5. All of Cases 1–4 do not occur.
Since |V(T)|≥4 and Case 1 does not occur, T is not a path. So T has at least one vertex of degree at least 3.
Claim 5.1. There does not exist a vertex u adjacent to three end-vertices in T.
Suppose not. Let v1 be an end-vertex which is adjacent to u in T and let T0=T−v1. By Observation 2.2, u is a fixed vertex of T0, which is contrary to the supposition that Case 2 does not occur.
Claim 5.2. There does not exist a vertex u linked with one 1-pendant path P1 and one 2-pendant path P2 in T.
Suppose not. Let V(P2)={x,y} with ux∈E(T). By Observation 2.3, there exists Du∈MDS_(T) such that u∈Du. Let D∗u=(Du−{x,y})∪{y}. Then D∗u−{y} is a dominating set of T−y, which implies that y is a critical vertex of T, contradicting the known condition that T has no critical vertices.
Claim 5.3. T has at least two vertices of degree at least 3.
Suppose, to the contrary, that T has only one vertex c with dT(c)≥3. By Lemma 2.7, c is linked with |NT(c)| pendant paths in T. Since Case 1 does not occur, it follows from Claims 5.2 and 5.1 that all of these |NT(c)| pendant paths are 2-pendant paths. But this contradicts the supposition that Case 4 does not occur.
Claim 5.4. If u and v are two vertices of degree at least 3 in T such that dT(u,v)= max {dT(x,y)|both x and y are vertices of degrees at least 3 in T}, then |NT(u)|=3 and u is adjacent to 2 end-vertices in T.
By Lemma 2.8, u is linked with |NT(u)|−1 pendant paths in T. Since Cases 1 and 4 does not occur, it follows from Claims 5.2 and 5.1 that |NT(u)|=3 and u is adjacent to 2 end-vertices in T.
Now, let u and v be two vertices of T satisfying the supposition of Claim 5.4. Suppose that v1 and w1 are two end-vertices which are adjacent to u in T and NT(u)−{v1,w1}={r}. By Claim 5.4, the equivalent status of v and u, and Observation 2.2, we get that v is a fixed vertex of T−{u,v1,w1}. Since Case 3 does not occur, we have r≠v.
Let Tv be the component of T−r such that v∈V(Tv), {z}=NT(r)∩V(Tv), NT(r)−{z}={u1,u2,…,uq} (where u1=u) and Tu1,Tu2,…,Tuq be the components of T−r such that ui∈V(Tui) for every 1≤i≤q. Furthermore, we may suppose without loss of generality that Tu1,Tu2,…,Tul are not pendant paths of T as well as Tul+1,Tul+2,…,Tul+m are pendant paths of T, where 1≤l≤q and l+m=q.
Claim 5.5. Tui is a 2-pendant path of T for every l+1≤i≤l+m.
Suppose, to the contrary, that Tui′ is a pendant path of T with |V(Tui′)|≠2 for some l+1≤i′≤l+m. By Lemma 3.1, r is a non-critical vertex of T−V(Tui′). Since Case 1 does not occur, we have |V(Tui′)|=1. Let V(Tui′)={w} and T0=T−{u,v1,w1}. By Observations 2.2 and 2.3, one may let Dr∈MDS_(T) with u,r∈Dr. We claim that Dr∩V(T0)∈MDS_(T0). Otherwise there exists D0∈MDS_(T0) such that |D0|<|Dr∩V(T0)|. But then {u}∪D0 would be a dominating set of T with |{u}∪D0|<|{u}∪(Du∩V(T0))|=|Dr|, contradicting the minimality of |Dr|. Thus γ(T)=|Dr|=|{u}|+|Dr∩V(T0)|=1+γ(T0). Since Case 3 does not occur, r is not a fixed vertex of T0. Let ˆDr0∈MDS_(T0) with r∉ˆDr0. Then w∈ˆDr0 and {u}∪ˆDr0∈MDS_(T). Since ({u}∪ˆDr0)−{w} is a dominating set of T−w, it follows that w is a critical vertex of T, a contradiction.
Claim 5.6. For every 2≤i≤l, ui is the unique vertex of V(Tui) satisfying dT(ui)≥3.
Firstly, since Tui is not a pendant path of T, Tui has a vertex with degree at least 3 in T. Secondly, we claim that for every h∈V(Tui)−{ui}, h is not a vertex of V(Tui) with degree at least 3 in T. Otherwise, we have dT(h,v)=dT(h,ui)+dT(ui,v)>dT(ui,v)=1+dT(r,v)=dT(u,v), contradicting the selection of u and v. From these two observations, Claim 5.6 follows.
Since dT(ui,v)=dT(u1,v), we have |NT(ui)|=3 and ui is adjacent to 2 end-vertices in T for every 2≤i≤l by Claim 5.4, which implies that
T[{r}∪l⋃i=1V(Tui)∪m⋃j=1V(Tul+j)]≅Rl,m. |
(See Figure 5.) Let T0=T−({r}∪⋃li=1V(Tui)∪⋃mj=1V(Tul+j)). Then T=T0∽Rl,m. By Lemma 3.6 (b), T0 has no critical vertices. Thus we have T0∈T by the induction hypothesis, and so T∈T.
In conclusion, the result is true when |V(T)|=k. The necessity follows.
We think that it is quite difficult to give a construction for graphs without critical vertices. For further studies, ones may consider to characterize unicyclic graphs without critical vertices, or graphs with domination number 3 and without critical vertices.
1. National Natural Science Foundation of China (no. 12061047);
2. Natural Science Foundation of Jiangxi Province (no. 20192BAB211002);
3. Undergraduate Innovation Training Project of Hubei Province (no. 202111072011);
4. Foundation of Cultivation of Scientific Institutions of Jianghan University (no. 06210033).
The authors declared that they have no conflicts of interest to this work.
[1] |
Harris S (2013) Climatic change: Casual correlations over the last 240 Ma. Sci Cold Arid Reg 5: 259–274. doi: 10.3724/SP.J.1226.2013.00259
![]() |
[2] | Imbrie J, Imbrie J (1980) Modeling climatic response to orbital variations. Science 4: 943–953. |
[3] | Jin H, Cheng X, Lou D, et al. (2016) Evolution of permafrost in Northeast China since the Late Pleistocene. Sci Cold Arid Reg 8: 269–296. |
[4] | Harris S, Jin, He R, et al. (2018) Tessellons, topography, and glaciations on the Qinghai-Tibet Plateau. Sci Cold Arid Reg 10: 187–206. |
[5] | Strahler A (1969) Physical Geography, 3Eds., New York: J. Wiley and Sons. |
[6] | Wallen R (1992) Introduction to Physical Geography. Dubuque: Wm. C. Brown Publishers. |
[7] |
Rossby CG, et al. (1939) Relation between variations in the intensity of the zonal circulation of the atmosphere and the displacements of the semi-permanent centers of action. J Mar Res 2: 38–55. doi: 10.1357/002224039806649023
![]() |
[8] | Harris S (2010) Climatic change in Western North America during the last 15,000 years: The role of changes in the strengths of air masses in producing the changing climates. Sci Cold Arid Reg 2: 371–383. |
[9] | Harris S, Brouchkov A, Cheng G (2017) Geocryology. Characteristics and use of Frozen Ground and Permafrost Landforms, Baton Rouge, Florida: CRC Press. |
[10] |
Held I (2001) The portioning the tropical of the poleward energy transport between the tropical ocean and atmosphere. J Atmos Sci 58: 943–948. doi: 10.1175/1520-0469(2001)058<0943:TPOTPE>2.0.CO;2
![]() |
[11] |
Farneti R, Vallis G (2013) Meridional energy transport in the coupled atmosphere-ocean system: Compensation and partitioning. J Climate 26: 7151–7165. doi: 10.1175/JCLI-D-12-00133.1
![]() |
[12] |
Kang S, Shin Y, Codron F (2018) The partitioning of poleward energy transport response between the atmosphere and Ekman flux to prescribed surface forcing in a simplified GCM. Geosci Lett 5: 22. doi: 10.1186/s40562-018-0124-9
![]() |
[13] | Wu CY (1985) Flora Xizancica. Science Press, Volume 5, In Chinese. |
[14] | Charkevicz S (1985) Plantae Vasculares Orienttis Sovietici. Leningrad: Nauka, 8 volumes, In Russian. |
[15] | Krasnoborov I (1988) Flora Sibirae. Novosibirsk: Nauka. 13 volumes. In Russian. |
[16] | Breckle SW, Hedge I, Rafiqpoor M, et al. (2013) Vascular Plants of Afghanistan. Bonn: Scientia Bonnensis. |
[17] | Harris S (1982) Cold air drainage west of Fort Nelson, British Columbia. Arctic 35: 537–541. |
[18] | NSIDC, New study explains Antarctica's coldest temperatures. 2018. Available from: https://nsidc.org/news/newsroom/new-study-explains-antarctica-coldest-temperatures. |
[19] |
Arnfield A (2003) Two decades of urban climate research: A review of turbulence, exchanges of energy and water and the heat island. Int J Climatol 23: 1–26. doi: 10.1002/joc.859
![]() |
[20] |
Østrem G (1966) The height of the glaciation limit in southern British Columbia and Alberta. Geogr Ann A 48: 126–138. doi: 10.1080/04353676.1966.11879734
![]() |
[21] | Sherzer W (1913) Glacial history of the Huron-Erie Basin: Geological report on Wayne County.In: Michigan Geological and Biological Survey, Lansing, Michigan: Wyakoop, Hallenbeck, Crawford Co., State printers Publishers. |
[22] | Shackleton N, Hall M, Pate D (1995) Pliocene stable isotope stratigraphy of site 846. Proc Ocean Drill Program: Sci Results 138: 337–353. |
[23] |
Harris S (1994) Chronostratigraphy of Glaciations and Permafrost episodes in the Cordillera of North America. Prog Phys Geog 18: 366–395. doi: 10.1177/030913339401800305
![]() |
[24] | Zheng B, Shen Y, Jiao K, et al. (2014) New progress and problems of Quaternary moraine dating in the Tibetan Plateau. Sci Cold Arid Reg 6: 183–189. |
[25] | Zhang H, Chang F, Li H, et al. (2018) OSL and AMS 14C age of the most complete mammoth fossil skeleton from northeastern China and itspaleoclimate significance. Radiocarbon 61: 347–358. |
[26] |
Vandenburghe J, Wang X, Vandenburghe D (2016) Very large cryoturbation structures of the last permafrost maximum age at the foot of the Qilian Mountains (NE Tibet Plateau, China). Permafrost Periglac 27: 138–143. doi: 10.1002/ppp.1847
![]() |
[27] |
Harris S, Jin H, He R (2017) Very Large cryoturbation structures of last permafrost maximum age at the foot of Qilian Mountains (NE Tibet Plateau, China): A discussion. Permafrost Periglac 28: 757–762. doi: 10.1002/ppp.1942
![]() |
[28] |
Voris H (2000) Maps of Pleistocene sea levels in Southeast Asia: Shorelines, river systems and time durations. J Biogeogr 27: 1153–1167. doi: 10.1046/j.1365-2699.2000.00489.x
![]() |
[29] | Harris S, Jin H (2012) Tessellons and "sand wedges" on the Qinghai-Tibet Plateau and their palaeoenvironmental implications. Proceedings of the 10th International Conference on Permafrost, Salekhard, Russia, 1: 147–153. |
[30] | Yu L, Lai Z (2012) OSL Chronology and palaeoclimatic implications of aeolian sediments in the eastern Qaidam Basin of the northeastern Qinhai-Tibetan Plateau. Palaeogeogr Palaeocl 337–338: 120–129. |
[31] |
Liu B, Jin H, Sun L, et al. (2013) Holocene climatic change revealed by aeolian deposits from the Gonghe Basin, northeastern Qinghai-Tibetan Plateau. Quatern Int 296: 231–240. doi: 10.1016/j.quaint.2012.05.003
![]() |
[32] |
Yang S, Jin H (2011) δ18O and δD records of inactive ice-wedges in Yitulihe, Northeast China and their paleoclimatic implications. Sci China Earth Sci 54: 119–126. doi: 10.1007/s11430-010-4029-5
![]() |
[33] |
Yang S, Cao X, Jin H (2015) Validation of wedge ice isotopes at Yituli'he, northeastern China as climate proxy. Boreas 44: 502–510. doi: 10.1111/bor.12121
![]() |
[34] |
Tarasov P, Bezrukova E, Karabanov E, et al. (2007) Vegetation and climate dynamics during the Holocene and Eemian interglacials derived from Lake Baikal pollen records. Palaeogeogr Palaeocl 252: 440–457. doi: 10.1016/j.palaeo.2007.05.002
![]() |
[35] |
Tarasov P, Bezrukova E, Krivonogov S (2009) Late Glacial and Holocene changes in vegetation cover and climate in Southern Siberia derived from a 15 kyr long pollen record from Lake Kotokel. Clim Past 5: 285–295. doi: 10.5194/cp-5-285-2009
![]() |
[36] |
Murton J, Edwards M, Lozhkin A, et al. (2017) Preliminary paleoenvironmental analysis of permafrost deposits at Batagnika megaslump, Yana Uplands, northeast Siberia. Quaternary Res 87: 314–330. doi: 10.1017/qua.2016.15
![]() |
[37] | Lozhkin A, Anderson P (2018) Another perspective on the age and origin of the Berelyokh Mammoth site (northeast Siberia). Quaternary Res 9: 1–19. |
[38] |
Clague J, Curry B, Dreimanis A, et al. (1993) Initiation and development of the Laurentide and Cordilleran Ice Sheets following the last interglaciation. Quat Sci Rev 12: 79–114. doi: 10.1016/0277-3791(93)90011-A
![]() |
[39] | Prest V (1990) Laurentide ice-flow patterns: A historical review, and implications of the dispersal of Belcher Island erratics. Geogr phys Quatern 44: 113–136. |
[40] | Lemke R, Laird W, Tipton M, et al. (1965) Quaternary geology of the Northern Great Plains, In: Wright H.E., Jr., Frey, D.G. Editors, The Quaternary of the United States, Princeton: Princeton University Press, 15–27. |
[41] | Koerner R (2010) Glaciers of the Hugh Arctic Islands, In: Williams, R.S., Jr., Ferriguo, J.G. Editors, Satellite Image Atlas of Glaciers of The World, United States Geological Survey Professional Paper, 1486–J–1, J111–J–146. |
[42] |
Gooding A (1963) Illinoian and Wisconsin Glaciations in the Whitewater Basin, Southeast Indiana, and adjacent areas. J Geo 71: 665–682. doi: 10.1086/626948
![]() |
[43] | Frye J, Willman H, Black R (1965) Outline of glacial geology of Illinois and Wisconsin. In: Wright H.E., Jr., Frey, D.G. Editors, The Quaternary of the United States, Princeton: Princeton University Press, 43–61. |
[44] | Wayne W, Zumberge J (1965) Pleistocene geology of Indiana and Michigan, In: Wright H.E., Jr., Frey, D.G. Editors, The Quaternary of the United States, Princeton: Princeton University Press, 63–83. |
[45] | Goldthwait R, Dreimanis A, Forsyth J, et al. (1965) Pleistocene deposits of the Erie Lobe, In: Wright, H.E., Jr., Frey, D.G. Editors, The Quaternary of the United States, Princeton: Princeton University Press, 85–97. |
[46] |
Teller, JT, Fenton, MM (1980) Late Wisconsin Glacial stratigraphy and history of southeastern Manitoba. Can J Earth Sci 17: 19–35. doi: 10.1139/e80-002
![]() |
[47] |
Christiansen E (1992) Pleistocene stratigraphy of the Saskatoon area, Saskatchewan, Canada: An update. Can J Earth Sci 29: 1767–1778. doi: 10.1139/e92-139
![]() |
[48] | SkwaraWoolf T (1980) Mammals of the Riddell Local Fauna (Floral Formation, Pleistocene, Late Rancholabrean) Saskatoon, Canada. Saskatoon: Culture and Youth Museum of Natural History, Regina. |
[49] | Dyke A (2004) An outline of North American deglaciation with emphasis on Central and northern Canada. In: Ehlers, J., Gibbard P.L. Editors, Quaternary glaciations–Extent and Chronology, Part II. Amsterdam: Elservier Science and Technology Books. |
[50] |
Barendregt R, Irving E (1998) Changes in the extent of North American ice sheets during the Late Cenozoic. Can J Earth Sci 35: 504–509. doi: 10.1139/e97-126
![]() |
[51] |
Patton H, Hubbard A, Andreassen K, et al. (2017) Deglaciation of the Eurasian ice sheet complex. Quat Sci Rev 169: 148–172. doi: 10.1016/j.quascirev.2017.05.019
![]() |
[52] | Monegato G, Ravizzi C (2018) The Late Pleistocene multifold glaciation in the Alps: Update and open questions. Alp Mediterr Quat 31: 225–229. |
[53] |
Patterson C (1998) Laurentide glacial landscapes: The role of ice streams. Geology 26: 643–646. doi: 10.1130/0091-7613(1998)026<0643:LGLTRO>2.3.CO;2
![]() |
[54] | Dredge L, Thorleifson L (1987) The Middle Wisconsin history of the Laurentide ice sheet. Geogr phys Quatern 41: 215–235. |
[55] |
Liverman D, Catto N, Rutter N (1989) Laurentide glaciation in west-central Alberta: A single (Late Wisconsinan) event. Can J Earth Sci 26: 266–274. doi: 10.1139/e89-022
![]() |
[56] |
Young R, Burns J, Smith D, et al. (1994) A single, late Wisconsin Laurentide glaciation, Edmonton area and southwestern Alberta. Geology 22: 683–686. doi: 10.1130/0091-7613(1994)022<0683:ASLWLG>2.3.CO;2
![]() |
[57] | Jackson L, Little E (2004) A single continental glaciation of Rocky Mountain Foothills, south-western Alberta, Canada. Dev Quatern Sci 2: 29–38. |
[58] | Andriashek L, Barendregt R (2016) Evidence for Early Pleistocene glaciation from borehole stratigraphy in north-central Alberta, Canada. Can J Earth Sci 54: 445–460. |
[59] |
Marshall S, Clarke K, Dyke A, et al. (1996) Geologic and topographic controls on fast flow in the Laurentide and Cordilleran ice sheets. J Geophys Res 101: 17827–17839. doi: 10.1029/96JB01180
![]() |
[60] |
Margold M, Stokes C, Clark C (2015) Ice streams in the Laurentide Ice Sheet: Identification, characteristics and comparison to modern ice sheets. Earth-Sci Rev 143: 117–146. doi: 10.1016/j.earscirev.2015.01.011
![]() |
[61] | Henderson E (1959) Surficial geology of Sturgeon Lake map-area, Alberta. Geol Surv Can Memoir 303. |
[62] | Tokarsky O (1967) Geology and groundwater resources (Quaternary) of the Grimshaw area, Alberta (Canada). Unpublished M.Sc. thesis, University of Alberta, Edmonton. |
[63] | St. Onge D (1972) La stratigraphie du quaternaire des environs de Fort-Assiniboine, Alberta, Canada. Rev Géogr Montreal 26: 153–163. |
[64] | Alley N (1973) Glacial stratigraphy and limits of the Rocky Mountain and Laurentide ice sheets in southwestern Alberta, Canada. B Can Petrol Geol 21: 153–177. |
[65] |
Alley N, Harris S (1974) Pleistocene Glacial Lake sequence in the Foothills, southwestern Alberta, Canada. Can J Earth Sci 11: 1220–1235. doi: 10.1139/e74-115
![]() |
[66] | Stalker A (1976) Quaternary stratigraphy of the southwestern Canadian Prairies. In: Mahoney, W.C. Editor, Quaternary Stratigraphy of North America, Strodsberg, Pennsylvania, 381–407. |
[67] | Mathews W (1978) Quaternary stratigraphy and geomorphology of Charlie Lake (94A) map area, British Columbia. Geol Surv Can 76–20. |
[68] | Duk-Rodkin A, Barendregt R, Tarnocai C, et al. (1995) Late Tertiary to late Quaternary record in the Mackenzie Mountains, Northwest Territories, Canada: Stratigraphy, paleosols, paleomagnetism, and chlorine-36. Can J Earth Sci 33: 875–895. |
[69] |
Bednarski J, Smith T (2007) Laurentide and montane glaciation along the Rocky Mountain Foothills of northeastern British Columbia. Can J Earth Sci 44: 445–457. doi: 10.1139/e06-095
![]() |
[70] | Clayton L (1967) Stagnant glacier features of the Missouri Coteau. In: Clayton L., Freers T. Editors, Glacial Geology of the Missouri Coteau and adjacent areas. North Dakota Geological Survey Miscellaneous Papers, 30: 25–46. |
[71] | Prest V, Grant D, Rampton V (1968) Glacial Map of Canada. Geological Survey of Canada Map 1253A. |
[72] | Ryder J, Fulton R, Clague J (1991) The Cordilleran Ice Sheet and the glacial geomorphology of southern and central British Columbia. Geogr phys Quatern 45: 356–377. |
[73] | Fulton R (1991) A conceptual model for growth and decay of the Cordilleran Ice Sheet. Geogr phys Quatern 45: 281–286. |
[74] |
Nichol C, Monahan P, Fulton R, et al. (2015) Quaternary stratigraphy and evidence for multiple glacial episodes in the north Okanagan valley, British Columbia. Can J Earth Sci 52: 338–356. doi: 10.1139/cjes-2014-0182
![]() |
[75] | Jackson L, Clague, J (1991) The Cordilleran Ice Sheet: One hundred and fifty years of exploration and discovery. Geogr phys Quatern 45: 269–280. |
[76] |
Harris S (1985) Evidence for the nature of the early Holocene climate and paleogeography, High Plains, Alberta, Canada. Arct Alp Res 17: 49–67. doi: 10.2307/1550961
![]() |
[77] | Jackson L (1977) Quaternary stratigraphy and terrain inventory of the Alberta portion of the Kananaskis Lakes 1:250,000 sheet (82-J), Unpublished Ph.D. thesis, University of Calgary, Calgary. |
[78] |
Jackson L (1980) Glacial history and stratigraphy of the Alberta portion of the Kananaskis Lake map area. Can J Earth Sci 17: 459–477. doi: 10.1139/e80-043
![]() |
[79] | Borns H (1973) Late Wisconsin fluctuations of the Laurentide ice sheet in southern and eastern New England. Geol Soc Am Bull 139: 37–45. |
[80] |
Mulligan R, Bajc A (2018) The pre-Late Wisconsin stratigraphy of southern Simcoe County, Ontario: Implications for ice sheet buildup, decay and Great Lakes drainage evolution. Can J Earth Sci 55: 709–729. doi: 10.1139/cjes-2016-0160
![]() |
[81] |
Christiansen E (1979) The Wiscosin deglaciation of southern Saskatchewan and adjacent areas. Can J Earth Sci 16: 913–938. doi: 10.1139/e79-079
![]() |
[82] | Upham W (1895)The Glacial Lake Agassiz; Monographs of the United States Geological Survey, Volume XXV, Washington.D.C.: Government Printing Office. |
[83] | Teller J, Clayton L (1983) Glacial Lake Agassiz. Geological Association of Canada, St. Johns, Newfoundland. |
[84] |
Teller J (1990) Volume and routing of late-glacial runoff from the southern Laurentide Ice Sheet. Quaternary Res 34: 12–23. doi: 10.1016/0033-5894(90)90069-W
![]() |
[85] |
Fisher, T, Smith D, Andrews J (2002) Preboreal oscillation caused by a glacial Lake Agassiz flood. Quat Sci Rev 21: 873–878. doi: 10.1016/S0277-3791(01)00148-2
![]() |
[86] |
Teller J, Leverington D (2004) Glacial Lake Agassiz: A 5000 yr history of change and its relationship to the δ18O record of Greenland. GSA Bull 116: 729–742. doi: 10.1130/B25316.1
![]() |
[87] |
Churcher C (1968) Pleistocene ungulates from the Bow River gravels at Cochrane, Alberta. Can J Earth Sci 5: 1467–1488. doi: 10.1139/e68-145
![]() |
[88] |
Churcher C (1975) Additional evidence of Pleistocene ungulates from the Bow River gravels at Cochrane, Alberta. Can J Earth Sci 12: 68–76. doi: 10.1139/e75-008
![]() |
[89] |
Wilson M, Churcher C (1978) Late Pleistocene Camelops from the Gallelli Pit, Calgary, Alberta: Morphology and geologic setting. Can J Earth Sci 15: 729–740. doi: 10.1139/e78-080
![]() |
[90] |
Ritchie J (1976) The Late Quaternary vegetational history of the western interior of Canada. Can J Bot 54: 1793–1818. doi: 10.1139/b76-194
![]() |
[91] |
MacDonald G (1982) Late Quaternary paleoenvironments of the Morley Flats and Kananaskis Valley of southwestern Alberta. Can J Earth Sci 19: 23–35. doi: 10.1139/e82-003
![]() |
[92] | Gryba EM (1983) Sibbald Creek: 11,000 years of Human Use of the Alberta Foothills. Archaeological Survey of Alberta, Occasional Paper #22. |
[93] | Luckman B (1988) 8200-year-old-wood from the Athabasca Glacier, Alberta. Can J Earth Sci 14: 1809–1822. |
[94] |
Osborn G, Luckman B (1988) Holocene glacier fluctuations in the Canadian (Alberta and British Columbia). Quat Sci Rev 7: 115–128. doi: 10.1016/0277-3791(88)90002-9
![]() |
[95] | Harris S, Howell J (1977) Chateau Lake Loiuse moraines–evidence for a new Holocene glacial event in southwestern Alberta. B Can Petrol Geol 25: 441–455. |
[96] | Zoltai S, Tarnocai C, Pettapiece W (1978) Age of cryoturbated organic materials in earth hummocks from the Canadian Arctic. In: Proceedings of the 3rd International Conference on Permafrost, Edmonton, Alberta. Ottawa, National Research Council of Canada: 326–331. |
[97] | Harris S (2002) Biodiversity of the vascular timberline flora in the Rocky Mountains of Alberta, Canada. In: Koerner, C., Spehn, E. Editors, Mountain Biodiversity: A global assessment, Lancashire: Parthenon Publishing group, United Kingdom, 49–57. |
[98] |
Fontanella F, Feldman C, Siddall M, et al. (2008) Phylogeography of Diadophis puntatus: Extension lineage diversity and repeated patterns of historical demography of a trans-continental snake. Mol Phylogenet Evol 46: 1049–1070. doi: 10.1016/j.ympev.2007.10.017
![]() |
[99] | Harris S (2012) The role that diastrophism and climatic change have played in determining biodiversity in continental North America. In: Lameed, A. Editor, Biodiversity, Conservation and Utilization in a Diverse World, Intech Press, 233–260. |
[100] | Zagura S (1984) The initial peopling of the Americas: an overview from the perspective of physical anthropology. Acta Anthropog 8: 1–21. |
[101] |
Kitchen A, Miyamoto M, Mulligan C (2008) A three stage colonization model for the peopling of the Americas. PLOS ONE 3: e1596. Available from: Doi.org/10.1371/journal.pone.0001596. doi: 10.1371/journal.pone.0001596
![]() |
[102] | Fagan B (2016) Searching for the origins of the first Americans. Sapiens. |
[103] | Anon (2018) Suspected first trace of Beringian people on the land bridge – now mostly sunken – joining Russia and North America. The Siberian Times. |
[104] |
Williams R, Steinberg A, Gershowitz H, et al. (1985) GM allotypes in Native Americans: Evidence for three distinct migrations across the Bering land bridge. Am J Phys Anthropol 66: 1–19. doi: 10.1002/ajpa.1330660102
![]() |
[105] |
Goebel T, Waters M, Dikova M (2003) The archaeology of Ushki Lake, Kamchatka, the Pleistocene peopling of the Americas. Science 301: 501–505. doi: 10.1126/science.1086555
![]() |
[106] |
Elias S, Crocker B (2008) The Bering Land Bridge: A moisture barrier to the dispersal of steppe-tundra biota? Quat Sci Rev 27: 2473–2483. doi: 10.1016/j.quascirev.2008.09.011
![]() |
[107] |
Murton J, Goslar T, Edwards M, et al. (2015) Palaeoenvironmental interpretation of Yedoma Silt (Ice Complex) deposition as cold-climate loess, Duvenny Yar, Northeast Siberia. Permafrost and Periglac 26: 208–288. doi: 10.1002/ppp.1843
![]() |
[108] | Madsen D, Perreault C, Rhode D, et al. (2017) Early foraging settlement of the Tibetan Plateau Highlands. Archaeol Res Asia. |
[109] | Sanchez G, Holliday V, Gaines E, et al. (2014) Human (Clovis)–gomphothere (Cuvieronius sp.) association ∼13,390 calibrated yBP in Sonora, Mexico. PNAS 111: 10972–10977. |
[110] | Ferring C (2001) The Archaeology and Paleoecology of the Aubrey Clovis Site (41DN479), Denton County, Texas. U.S. Army Corps of Engineers, Fort Worth District. Center for Environmental Archaeology, Department of Geography, University of North Texas. |
[111] |
Goebel T, Waters M, O'Rourke D (2008) The late Pleistocene dispersal of modern humans in the Americas. Science 319: 1497–1502. doi: 10.1126/science.1153569
![]() |
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